- About this Journal
- Abstracting and Indexing
- Aims and Scope
- Article Processing Charges
- Articles in Press
- Author Guidelines
- Bibliographic Information
- Citations to this Journal
- Contact Information
- Editorial Board
- Editorial Workflow
- Free eTOC Alerts
- Publication Ethics
- Reviewers Acknowledgment
- Submit a Manuscript
- Subscription Information
- Table of Contents
Advances in Meteorology
Volume 2010 (2010), Article ID 756071, 15 pages
Impacts of Oceanic Preexisting Conditions on Predictions of Typhoon Hai-Tang in 2005
Meteorological Research Institute, 1-1 Nagamine, Tsukuba, Ibaraki 305-0052, Japan
Received 31 December 2009; Revised 13 April 2010; Accepted 27 May 2010
Academic Editor: Zhaoxia Pu
Copyright © 2010 Akiyoshi Wada and Norihisa Usui. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.
We investigated the impact of variations in oceanic preexisting conditions on predictions of Typhoon Hai-Tang (2005) by using a coupled atmosphere-ocean model with 6-km horizontal resolution and providing the oceanic initial conditions on 12 July from 1997 to 2005 to the model. Variations in oceanic preexisting conditions caused variation in predicted central pressure of nearly 18 hPa at 72 h, whereas sea-surface cooling (SSC) induced by Hai-Tang caused a predicted central pressure difference of about 40 hPa. Warm-core oceanic eddies up to a few hundred kilometers across and a deep mixed layer climatologically distributed in the western North Pacific led to high mixed-layer heat potential, which increased latent heat flux, water vapor, and liquid water contents around Hai-Tang's center. These increases were closely associated with Hai-Tang's intensification. SSC negatively affected the eyewall, whereas variations in oceanic preexisting conditions remarkably affected spiral rainbands and the magnitude of SSC.
Advances in ocean data assimilation systems have enabled us to further understand tropical cyclone (TC) activity and the ocean response at weather-forecasting as well as seasonal to climate time scales. The relationships between TC activity and variations in the global ocean are of growing interest on seasonal to climate time scales. In contrast, TC-induced sea-surface cooling (SSC), the decrease in sea-surface temperature (SST) during and after the passage of a TC in general, is a well-known ocean response to a TC on a weather-forecasting scale. Previous studies reported that SSC varied depending on oceanic preexisting conditions  as well as on TC intensity and translation speed . However, the dynamic and thermodynamic processes associated with SSC remain controversial [1, 3, 4] although vertical turbulent mixing and upwelling are known to be important . According to our current understanding of the relationship between TC activity and ocean thermal forcing, not only SST but also temperature and salinity profiles in the upper ocean are important for determining TC intensity, whereas SSC slightly affects TC track prediction .
TC heat potential (TCHP), a measure of the oceanic heat content from the surface to the C isotherm depth (Z26), is highly correlated with TC intensity in the western North Pacific (WNP) on seasonal to climate time scales [6, 7]. TCs tend to rapidly intensify in the WNP when they pass over a region with a high TCHP and a deep Z26. Providing accurate oceanic preexisting conditions as oceanic initial conditions to a coupled atmosphere-ocean model used for typhoon prediction is thus important if the model is to predict TCs precisely, particularly their intensity, but how oceanic preexisting conditions affect TC predictions is still unclear.
On a weather-forecasting scale, idealized numerical experiments have demonstrated that TC-induced SSC substantially affects TC intensity during its intensification phase but not during its mature phase . Rapid TC intensification during its intensification phase is caused by mesovortices, filamentation, and vortex Rossby waves enhanced by TC-scale cyclonic circulation. SSC in Wada , defined as a decrease in computed SST from the initial SST, plays a role in weakening mesovortices, which suppresses lower-tropospheric cooling by evaporation along spiral rainbands and the associated local anticyclonic flow around the mesovortices. The resulting relatively high central pressure then weakens the TC-scale cyclonic circulation. This negative feedback  reduces TC intensification.
The purpose of the present study was to quantitatively evaluate the impact of oceanic preexisting conditions on predictions of a TC during its intensification phase on a weather-forecasting time scale. We performed several numerical prediction experiments for Typhoon Hai-Tang (2005) by providing nine different oceanic initial conditions to a coupled atmosphere-ocean model. The initial conditions were determined from daily oceanic reanalysis data for 1997 to 2005 calculated by the North Pacific version of the Meteorological Research Institute (MRI) ocean variational estimation (MOVE) system .
This paper consists of five sections. Section 2 describes the model and the experiment design. Section 3 describes the results of numerical prediction experiments. Section 4 discusses the role of variation in oceanic preexisting conditions on predictions of TC intensity and the sensitivity of predictions of Hai-Tang’s intensity to upper-ocean variations on seasonal to climate time scales. Section 5 is the conclusion.
2. Model and Experiment Design
This section consists of four subsections. Section 2.1 explains the best-track data used in this study. Section 2.2 presents a summary of each component of the coupled atmosphere-ocean model. Section 2.3 outlines the experiment design. Section 2.4 defines mixed-layer heat potential.
2.1. Best-Track Data
To validate the results of the numerical prediction experiments described below, the best-track data of Hai-Tang’s positions and central pressures, archived by the Regional Specialized Meteorological Center , were used. Best-track data are defined as the sustained 10-min means. We used predicted central pressure to represent Hai-Tang’s predicted intensity.
2.2. Coupled Model
The nonhydrostatic atmosphere model coupled with the ocean model (NCM) consists of a nonhydrostatic atmosphere model (NHM)  and a mixed-layer ocean model [2, 8]. An oceanic sublayer scheme for calculating an increase in temperature in the upper-ocean skin layer  is included in the mixed-layer ocean model for calculating diurnally varying SST.
The NHM used in the present study is an older version of the nonhydrostatic mesoscale model developed for operational use at the Japan Meteorological Agency in collaboration with the MRI. Physical schemes incorporated into the NHM and NCM are an explicit three-ice bulk microphysics scheme  in conjunction with the Kain-Fritsch convective parameterization scheme , a resistance law assumed for sensible and latent heat fluxes and wind stress in the surface boundary layer; exchange coefficients for sensible and latent heat fluxes and wind stress over the sea, determined using Kondo’s  bulk formulas, a turbulent closure model in the atmospheric-boundary layer [16, 17], and an atmospheric radiation scheme .
2.2.2. Mixed-Layer Ocean Model
The mixed-layer ocean model is a reduced gravity model developed at the MRI [2, 8]. In the present study, the ocean model consists of three layers and four levels. The uppermost layer is a mixed layer with vertically uniform density. The middle layer is a seasonal thermocline and shows the largest vertical temperature gradient among the three layers. The bottom layer is assumed to be undisturbed by entrainment. Four levels consist of the surface, the base of the mixed layer/top of the thermocline, the base of the thermocline/top of the bottom layer, and the sea floor. Temperature and salinity are calculated only at the surface and at the base of the mixed layer, whereas layer thickness and oceanic flows are calculated for all layers. The water depth is limited to 2000 m. The mixed-layer depth is determined from oceanic reanalysis data by assuming a difference in density from the surface of no more than 0.25 g m−3 and it is limited to 200 m. The base of the thermocline is limited to 600 m.
2.2.3. Oceanic Sublayer Scheme
The specifications of the mixed-layer ocean model described in Section 2.2.2 are insufficient for realistic simulation of the amplitude of diurnal SST variations because of the thickness (1 m) of the mixed layer. To improve the simulation of diurnally varying SST, we incorporated into the mixed-layer ocean model an oceanic sublayer scheme that we developed following Schiller and Godfrey , but with short-wave absorption/penetration calculated using the formulation of Ohlmann and Siegel .
According to the algorithm of Schiller and Godfrey’s  scheme, a skin layer forms in the uppermost layer when short-wave radiation warms the sea surface. The thickness of the skin layer is determined from the total amount of short-wave radiation and the cumulative wind stress from sunrise to sunrise. Short-wave radiation and wind stress are provided by the NHM to the mixed-layer ocean model at every time step, but short-wave radiation and wind stress accumulate between sunrises only in the oceanic sublayer scheme. The thinner the skin layer is, the larger the amplitude of diurnal SST variation becomes. After sunset, the skin layer vanishes and its depth is reset to the reference depth (5 m in the present study). The total amounts of short-wave radiation and wind stress then remain constant within the oceanic sublayer scheme until next sunrise.
Ohlmann and Siegel  derived the formulas associated with short-wave absorption/penetration by multiple regression analysis. Short-wave absorption/penetration is a function of the chlorophyll-a concentration (mg m−3), the cloud index under cloudy conditions, and the solar zenith angle under clear-sky conditions. When the chlorophyll-a concentration is high, the amplitude of diurnal SST variations tends to be large .
2.3. Experiment Design
NHM and the mixed-layer ocean model each contain horizontal grids and the horizontal grid spacing is 6 km. NHM has 40 vertical levels, and the interval between levels varies from 40 m near the surface to 1180 m for the uppermost layer. The top height is nearly 23 km. The time step of the NHM is 12 s, and that of the mixed-layer ocean model is 72 s. Atmospheric and oceanic data are exchanged between the NHM and mixed-layer ocean model every 72 s as follows: the SST calculated in the mixed-layer ocean model is provided to the NHM as the surface boundary condition, and wind stress, short-wave and long-wave radiation, sensible and latent heat fluxes, and precipitation accumulated by the NHM during the time step of the ocean model (72 s) are provided to the mixed-layer ocean model as atmospheric forcing data.
To set the initial and boundary atmospheric conditions for the NHM and NCM, we first ran hydrostatic global spectral model (GSM) version T213L40 for 72 h. The horizontal resolution of GSM T213L40 is nearly 60 km. To avoid gaps in the horizontal resolution of downscale calculations, we next ran a hydrostatic regional spectral typhoon model (TYM) with a horizontal grid spacing of nearly 20 km at Hai-Tang’s initial position for 72 h. The TYM provided initial and boundary atmospheric conditions every 3 h based on the output of the GSM  to both the NHM and NCM. It should be noted that a bogus typhoon was incorporated only into the numerical prediction by the TYM, and that the effect of the bogus typhoon must be considered in the numerical prediction experiments of the NHM and NCM, because the initial atmospheric conditions for the NHM and NCM runs were based on the output of the TYM. Lateral boundary conditions created from the TYM output were also provided to NHM and NCM every 3 h. The integration time of GSM, TYM, NHM, and NCM was 72 h, starting from 1200 UTC 12 July 2005.
Oceanic initial conditions were obtained from daily oceanic reanalysis data with a horizontal grid spacing of from 1997 to 2005. Daily oceanic reanalysis data were calculated by the MOVE system . Table 1 lists the numerical prediction experiments conducted in the present study. We ran nine experiments with the NCM and another nine experiments with the NHM, not being coupled with the mixed-layer ocean model.
To investigate the impact of variations in oceanic preexisting conditions on predictions of Hai-Tang, nine separate sets of oceanic initial conditions were created from the daily oceanic reanalysis data of 12 July during 1997–2005 (Table 1). The nine oceanic initial conditions include some remarkable oceanic variations at seasonal to climate time scales: for example, 12 July 1999 was during a mature La Niña event, whereas 12 July 2002 was during a mature El Niño event; 12 July 2005 fell at the end of a central Pacific warming event during the transition to La Niña.
Hai-Tang was a super-typhoon, defined as a typhoon with maximum sustained 1-min-mean surface winds of 67 m s−1 or greater. According to the best-track data, Hai-Tang formed near N, E at 0000 UTC on 13 July 2005. Hai-Tang initially moved northwestward; then, after it entered the tropical cyclogenesis phase, it turned to move southwestward to westward while rapidly intensifying. Hai-Tang attained a central pressure of 920 hPa at 0600 UTC on 16 July. This study investigated Hai-Tang’s rapid-intensification phase, starting with the tropical cyclogenesis phase. Therefore, we set the initial integration time to 1200 UTC on 12 July 2005. We could not, however, reproduce the tropical cyclogenesis phase realistically in the present numerical prediction experiments because the bogus typhoon included in the initial atmospheric conditions negatively affected the prediction of Hai-Tang’s track, as described in Section 3.1. Therefore, we focused on the impact of variations in the oceanic preexisting conditions on predictions of Hai-Tang’s rapid intensification.
Hai-Tang passed over two warm-core eddies, characterized by a high sea-surface height (SSH) with a positive SSH anomaly (SSHA), a high TCHP, and a deep Z26, in the WNP as it rapidly intensified (Figure 1). Conversely, as it passed over the cold wake, it ceased to intensify and its best-track central pressure remained constant (Figure 1(a)). The warm-core eddy at around N, E (Figure 1(b)), where the SSH was high, was a few hundred kilometers across. The MOVE system reproduced this warm-core eddy (W1, Figure 1(c)) reasonably well, as well as the high SSH associated with the other warm-core eddy (W2, Figures 1(a) and 1(c)). Hai-Tang’s intensification was thus associated with these warm-core eddies.
2.4. Mixed-Layer Heat Potential
Here, we defined the mixed-layer heat potential (MLHP: kJ cm−2)  as where ρ is the density of sea water in the mixed layer underneath a TC, which is assumed to be constant; Cpis the specific heat at constant pressure; T1 is the SST underneath a TC; h1 is the mixed-layer depth (MLD) underneath a TC. The variables , T1, and h1 were obtained from daily oceanic reanalysis data.
2.5. Tropical-Cyclone Heat Potential
TCHP (kJ cm−2) is defined as where is the density of the sea water at each layer, Th is the sea temperature () at each layer, Zh is the thickness at each layer, H is the vertical level of depth corresponding to Z26, and h is the variable number of vertical levels based on the configuration of the ocean data reanalysis system described in Section 3. When Th is below , TCHP at the layer is assumed to be zero.
3.1. Track and Intensity Prediction
We first investigated the impact of variations in oceanic preexisting conditions on predictions of Hai-Tang’s track. Figure 2 depicts Hai-Tang’s best-track positions and the mean positions predicted by NHM and NCM (Table 1). Both predicted tracks show a marked northwestward bias during the early integration period, and they both subsequently turn southwestward. Thus, the track predictions did not significantly differ between NHM and NCM. At 72 h, the predicted tracks approach Hai-Tang’s best-track position. Table 2 lists the mean predicted positions for every 24 h and their standard deviations. The maximum standard deviation at 72 h, of longitude, is comparable to the difference of center position at 72 h between NHM and NCM, nearly of latitude (Table 2). Thus, variations in oceanic preexisting conditions had no significant impact on predictions of Hai-Tang’s track as well as a difference in predicted SSTs between NHM and NCM.
The impact of SSC on predictions of TC central pressure was remarkable, particularly during the later period of numerical integration . We investigated the evolution of the central pressures predicted by NCM (Figure 3(a)) and NHM (Figure 3(b)) along with their mean difference and standard deviations (Figure 3(c)). All of the central pressures predicted by NCM were higher than the best-track central pressure after 18 h (Figure 3(a)), whereas most central pressures predicted by NHM were lower (Figure 3(b)). The difference in predicted central pressure between NHM and NCM became significant after 24 h and small after 48 h (Figure 3(c)). The twofold standard deviation of the predicted central pressure difference was nearly 18 hPa at 72 h (Figure 3(c)). This value represents the amplitude of the variation in the predicted central pressure due to the variation in oceanic preexisting conditions. The amplitude of 18 hPa is less than the difference in predicted central pressure between NHM and NCM, which increased to more than 40 hPa at 72 h, suggesting that the impact of oceanic preexisting conditions on predictions of Hai-Tang’s intensity was smaller than the impact of the difference between NHM and NCM in the SST decrease caused by Hai-Tang’s passage.
3.2. Oceanic Responses
We defined SST as temperature at the first level of the mixed-layer model plus skin temperature calculated in the oceanic sublayer scheme and SSC as the decrease in predicted SST from the initial SST due to Hai-Tang’s passage hereafter. It should be noted that the initial SST does not change during the integration in the experiments by NHM. Therefore, the magnitude of SSC at a certain integration time was equal to the difference in SST at a certain integration time between NHM and NCM. We investigated the evolution of mean SST and SSC underneath Hai-Tang and their standard deviations to determine the impact of the variations in oceanic preexisting conditions on SSC (Figure 4). Mean SST was calculated as the average SST underneath Hai-Tang’s center position among the nine predictions by NCM. Each SSC value was calculated as the difference in predicted SST underneath Hai-Tang’s center position from the initial SST. Mean differences in both SST and SSC were calculated as the averaged differences between NHM and NCM in the predictions of the nine experiments. The minimum mean SST and the maximum mean decrease in SST became significant at around 18 h, when the difference in the predicted central pressures between NHM and NCM also became apparent. The twofold standard deviation associated with the variations in SST underneath Hai-Tang was nearly , and the standard deviation associated with the variations in SSC was nearly . The standard deviation was large from the initial time to 18 h as predicted Hai-Tang rapidly intensified. After 18 h, the rate of intensification decreased and SST underneath Hai-Tang began to increase; however, it remained lower than the initial SST underneath Hai-Tang even though it did not decrease monotonically during the passage. The trend of predicted SST underneath Hai-Tang obtained here differed from the result of an idealized numerical experiment  because SSC was sensitive to the variations in the oceanic preexisting conditions such as the spatial and temporal variations in the preexisting warm-core eddy.
To investigate the relationships between the preexisting warm-core eddies and the climatologically deep mixed layer and Hai-Tang’s intensification, we calculated MLHP underneath Hai-Tang every hour using (1) and investigated the evolution of mean central pressure and mean MLHP averaged over the nine NCM predictions and their standard deviations (Figure 5). Mean MLHP was calculated as the average in a grid box at Hai-Tang’s center. The trend of mean central pressure was negatively correlated with the trend of mean MLHP, implying that high MLHP underneath Hai-Tang was associated with Hai-Tang’s intensification. However, Hai-Tang’s predicted track bypassed the warm-core eddy where MLHP was relatively high. In other words, Hai-Tang passed over a relatively low MLHP area because of the significant northwestward track-prediction error. This track-prediction error led to an intensity-prediction error caused by the predicted passage over an area with different MLHP. This difference in MLHP caused the standard deviation of predicted central pressure to increase (Figure 5) as the integration time progressed.
We have already mentioned in Section 3.1 that the northwestward track-prediction error during the early integration, which was closely related to the bogus typhoon used in the TYM calculation, caused the predicted Hai-Tang to travel where MLHP was relatively low. In contrast, the best-track data indicated that Hai-Tang passed over the warm-core eddy between 12 h to 36 h (Figure 1). In fact, NCM and NHM predicted that Hai-Tang would pass over the warm area north of warm-core eddy W1 (Figure 1(c)) between 0 h and 24 h (Figure 5). The amplitude of the variations in MLHP (Figure 5) was relatively high compared with that of the analyzed TCHP variation, even though the high TCHP at 1800 UTC on 14 July (Figure 1) was reproduced by NCM. The overestimation of MLHP caused by the track-prediction error led to prediction of an excessive reintensification of Hai-Tang. This overestimation of MLHP affected Hai-Tang’s predicted central pressure continuously, not temporarily during the integration.
The horizontal distribution of mean MLHP averaged over the nine NCM predictions during 72 h and that of the standard deviation are shown in Figure 6. MLHP was significantly lower on the north side of Hai-Tang’s track, where the standard deviation was relatively high, implying that SSC was highly sensitive to variations in oceanic preexisting conditions. The standard deviation was high not only on the north side of Hai-Tang’s track but also around , and , E. The high standard deviation in these areas away from Hai-Tang’s track can be explained by seasonal to climate time scale variations of oceanic conditions. Figure 6 also indicated that Hai-Tang entered a high-MLHP area during the later integration, and, in fact, the time series of best-track central pressure shows remarkable intensification during this later integration time (Figures 3 and 5).
According to Wada and Usui , accumulated TCHP (ATCHP) was highly correlated with the minimum central pressure of TCs occurring from 1998 to 2004. ATCHP is defined as the summation of TCHP within a square around the TC center from the genesis to the phase first reaching the minimum central pressure every six hours, corresponding to the interval of TC best track data. Here, instead of ATCHP, we calculated accumulated MLHP (AMLHP) from the initial time to 72 h. We then investigated the relationship between AMLHP and predicted central pressure at 72 h among the nine NCM predictions (Figure 7). Interestingly, AMLHP underneath Hai-Tang decreased monotonically from 1997 to 2005, however, predicted minimum central pressure did not increase monotonically during the period. In particular, predicted minimum central pressure markedly decreased during the strong El Niño Southern Oscillation (ENSO) event from 1997 to 1999. In addition, the predicted minimum central pressure was relatively low in 2005 even though AMLHP was also low. Therefore, a high linear correlation between minimum central pressure and AMLHP cannot be assumed, a result that is not consistent with the findings of Wada and Usui . Thus, whether AMLHP and predicted minimum central pressure are correlated may depend on the oceanic preexisting conditions (Figure 7).
3.3. Atmospheric Impact
The energy source for TC genesis and intensification is moisture provided from the ocean to the atmosphere through latent heat flux. Thus, latent heat flux is an important metric for TC intensification. We investigated the horizontal distribution of the mean latent heat flux averaged over 72 h among the NCM experiments and that of its standard deviation (Figure 8). Note that the NCM outputs latent heat flux every hour. Mean latent heat flux was relatively small during the early integration owing to the relatively weak intensity of Hai-Tang, but the standard deviation was relatively high at around N, E because of the uncertainty of Hai-Tang’s predicted central position. The standard deviation became small as integration progressed, whereas the mean latent heat flux became high as Hai-Tang intensified. Figure 9 depicts time series of mean central pressure and mean latent heat flux and their standard deviations, with mean latent heat flux calculated as the average in a grid box at Hai-Tang’s center. The two trends are negatively correlated, similar to the trends of mean central pressure and mean MLHP (Figure 5), implying that the variation in latent heat flux is closely related to that in MLHP, although surface wind velocity is another important metric for estimating latent heat flux when Kondo’s  bulk formulas are used.
Next, we investigated the effect of variations in oceanic preexisting conditions on the horizontal distribution of mean latent heat flux at 72 h, averaged over the nine NCM and NHM predictions. The NCM result shows a wave-1 asymmetric distribution pattern of mean latent heat flux (Figure 10(a)), whereas NHM produced an axisymmetric distribution pattern (Figure 10(c)). The area of high mean latent heat flux west of the mean center position of predicted Hai-Tang corresponds to Hai-Tang’s mean direction of travel as predicted by NCM (Figure 2). The standard deviation of the latent heat flux predictions by NCM was high inside Hai-Tang’s eyewall, where the horizontal gradient of surface wind velocity was variable ahead of Hai-Tang’s direction of travel (Figure 10(b)), whereas the standard deviation of the NHM predictions was high behind Hai-Tang’s direction of travel (Figure 10(d)). The difference in the horizontal distributions of mean latent heat flux between NCM (Figure 10(a)) and NHM (Figure 10(c)) resulted from SSC. In fact, mean latent heat flux was remarkably reduced behind Hai-Tang in NCM (Figure 10(a)) where atmospheric conditions had stabilized (not shown). High latent heat flux can be attributed to both the high-velocity surface winds associated with Hai-Tang’s intensification (Figure 9) and high SST or mixed-layer temperature associated with high MLHP (Figure 5). This result suggests that not atmospheric thermostatics but atmospheric dynamics and oceanic preexisting conditions determined the distribution and amplitude of latent heat flux around Hai-Tang.
We then examined the horizontal distributions of mean hourly precipitation averaged over 72 h among the nine NCM experiments and of the standard deviation (Figure 11). Heavy precipitation was concentrated along Hai-Tang’s predicted track. High mean precipitation and larger standard deviations tended to be on the south side of Hai-Tang’s track. Thus, precipitation was high on the opposite side of Hai-Tang’s track to high MLHP standard deviations (Figure 6). Figure 12 depicts time series of mean central pressure and mean precipitation and their standard deviations. Mean precipitation was calculated as the average in a grid box at Hai-Tang’s center. Mean precipitation tended to increase as Hai-Tang intensified. We can infer that high MLHP led to increases in latent heat flux (Figures 5 and 9), which caused the enhanced release of latent in the troposphere and heavy precipitation (Figure 12). The impact of the variations in oceanic preexisting conditions on MLHP predicted by NCM can be widely seen not only around N, E and N, E but also around the area where MLHP decreased as a result of the SSC induced by Hai-Tang (Figure 6), whereas their impact on precipitation was mainly limited to the south side of Hai-Tang.
The horizontal distribution of mean precipitation at 72 h (Figure 13(a)) successfully captures its wave-1 asymmetric pattern, which is similar to the precipitation pattern observed by satellite (Figure 14). In contrast, the axisymmetric pattern near Hai-Tang’s center (Figure 14) is similar to the horizontal distribution of mean precipitation at 72 h predicted by NHM (Figure 13(c)). The heavy precipitation near Hai-Tang’s center (Figure 14) is not reproduced well (Figure 13(a)) owing to the weak intensity of Hai-Tang predicted by NCM (Figure 3(a)), but it is reproduced to some extent in the NHM prediction (Figure 13(c)). The standard deviation of predicted mean precipitation was high in both NCM (Figure 13(b)) and NHM (Figure 13(d)) where mean precipitation was also high. The impact of variations in oceanic preexisting conditions on precipitation was significant around the spiral rainband southeastward of Hai-Tang’s center. In contrast, the axisymmetric pattern of precipitation vanished as a result of SSC (Figure 13(a)), suggesting that the variation in oceanic preexisting conditions directly affected the intensity of precipitation over the spiral rainbands, and then the variation over the spiral rainbands affected in turn the intensity prediction. Although Wada  studied intensification caused by mesovortices on spiral bands, this study demonstrated for the first time that the intensification process is influenced by variations in oceanic preexisting conditions.
To investigate the impact of variations in oceanic preexisting conditions on precipitation and Hai-Tang’s intensification, we focused on the variations in mean specific humidity averaged from the surface to nearly 14 km height (Figure 15(a)), mean specific cloud plus specific rain averaged from the surface to nearly 6.5 km height (Figure 15(b)), and the mean hourly change in potential temperature caused by radiation averaged from nearly 6.5 km height to 14 km height (Figure 15(c)). These mean values were also averaged within a radius of 300 km from Hai-Tang’s predicted center and also over the nine NCM predictions. Figure 15 also depicts the variations in mean specific humidity, mean specific cloud plus specific rain, and mean hourly change in potential temperature caused by radiation in 1999, 2004, and 2005. Here, we consider specific humidity to represent the water vapor content, and specific cloud plus rain to represent the liquid water content.
Variations in oceanic preexisting conditions began to cause significant variation in the water vapor content around predicted Hai-Tang at 12 h. The standard deviation increased during the early integration and reached a maximum at around 30 h. After 36 h, the standard deviation of the liquid water content around predicted Hai-Tang increased rapidly. Both water vapor and liquid water contents increased around predicted Hai-Tang as the predicted Hai-Tang intensified, suggesting that they can be regarded as the energy source for TC intensification. The impact of variations in oceanic preexisting conditions on the hourly change in potential temperature caused by radiation became significant after 36 h (Figure 15(c)), corresponding in timing to Hai-Tang’s intensification, as a result of variations in Hai-Tang’s atmospheric warm-core temperature caused by latent heat release. The difference in predicted central pressures among the nine NCM predictions became large at 24 h (Figure 3(a)) when the difference in hourly change in potential temperature caused by radiation began to appear significantly (Figure 15(c)). Predicted central pressure tended to be lower when the amplitude of diurnal variations in the hourly change in potential temperature caused by radiation was larger. The relationship was particularly marked when the oceanic preexisting conditions in 1999 were used as the initial oceanic conditions in NCM (NC99 in Table 1).
In contrast, water vapor content was markedly lower when oceanic preexisting conditions in 2004 were used as the initial oceanic conditions in NCM (NC04 in Table 1) compared with when the preexisting conditions of other years were used (Figure 15(a)). AMLHP predicted by NCM was lower in 2004 than that in any other year except 2005 (Figure 7). Liquid water content was also low at around 30 h and from 45 to 54 h in NC04 (Figure 15(b)). Lower water vapor and liquid water contents were associated with less variation in the hourly change in potential temperature caused by radiation. Thus, Hai-Tang’s central pressures predicted by NHM and NCM were particularly high when the oceanic preexisting conditions in 2004 were used as the initial oceanic conditions in the models. Therefore, the oceanic preexisting conditions associated with high MLHP around Hai-Tang’s track were more favorable for Hai-Tang’s intensification, because both MLHP and Hai-Tang’s surface winds played a crucial role in enhancing water vapor and liquid water contents around Hai-Tang as well as latent heat release in the upper troposphere, which resulted in high value of the hourly change in potential temperature caused by radiation.
4.1. The Effect of Cumulus Parameterization
We clarified the uncertainty in TC intensity predictions caused by variations in oceanic preexisting conditions for Typhoon Hai-Tang (2005). We first demonstrated that Hai-Tang’s predicted intensity was closely related to the variation in MLHP. Warm-core eddies and the climatologically deep mixed layer in the WNP played a crucial role in the intensification of Hai-Tang. We next demonstrated that water vapor and liquid water contents around Hai-Tang’s center increased when predicted Hai-Tang intensified over high MLHP areas, indicating a close relationship between MLHP and water vapor and liquid water contents. However, the Kain-Fritsch cumulus parameterization scheme  incorporated into the NHM and NCM might have contributed to these results, even though similar results were obtained by experiments with NHM and NCM when the Kain-Fritsch’s cumulus parameterization scheme was not used (not shown). Hai-Tang’s central pressures predicted by the NHM and NCM without using the Kain-Fritsch’s cumulus parameterization scheme were higher at the 6-km horizontal resolution than those predicted with the use of the Kain-Fritsch scheme (not shown) and far from the best-track central pressures. Therefore, in the present study we concluded that cumulus parameterization is required even at the 6-km resolution to reproduce Hai-Tang’s intensity realistically. In fact, the Kain-Fritsch’s cumulus parameterization scheme is closely associated with the local Convective Available Potential Energy (CAPE). CAPE is sensitive to the local thermostatic profile in the atmospheric boundary layer, enthalpy flux, and thus SST. Thus, cumulus convection as calculated by Kain-Fritsch’s cumulus parameterization is sensitive to SST. This implies that the Kain-Fritsch’s cumulus parameterization possibly changes not only central pressure predictions but also the distribution patterns of latent heat flux and precipitation intensity at around Hai-Tang’s predicted center. This study does not explore the sensitivity any further.
The impact in variations in oceanic preexisting conditions on precipitation intensities on the spiral rainbands of the typhoon (Figure 13) is qualitatively consistent with the results of cloud-resolving numerical experiments  that SSC suppresses mesovortices along the spiral bands. This suggests that precipitation intensities on the spiral rainbands around Hai-Tang are sensitive to variations in oceanic preexisting conditions. However, the impact of oceanic preexisting conditions on precipitation intensities on the spiral rainbands still requires quantitative evaluation because of the uncertainties associated with the cumulus parameterization. To explore the relationships among MLHP, water vapor plus liquid water contents, and Hai-Tang’s intensity, another numerical-prediction experiment with a grid spacing of 1 to 2 km, should be performed with a coupled atmosphere-ocean model that does not include cumulus parameterization. Although such experiments would improve TC intensity prediction, many computational resources would be needed to carry them out.
The evolution of SST, and SSC in particular, was associated with the variations in oceanic preexisting conditions  as well as with Hai-Tang’s intensity and translation . The magnitude of SSC in this study tended to be larger than that obtained in the previous study , partly because of the northwestward track error. In addition, we must pay attention to the possibility that the tuning parameter associated with breaking surface waves in the mixed-layer formulation [2, 8] may be too high. High tuning parameter values lead to excessive vertical turbulent mixing near the surface because of breaking surface waves, which enhances SSC . We thus need to improve the tuning parameter associated with breaking surface waves in the entrainment formulation  using the result of a coupled atmosphere-wave-ocean model.
The results of the numerical experiments of this study include the impact of diurnally varying SST in the upper-ocean skin layer on TC intensity prediction, but we could not separate the impact of sea-surface skin temperature variations on TC intensity prediction from that of oceanic preexisting conditions. Another numerical-prediction experiment without the upper-ocean skin-temperature scheme is needed to determine the separate impact of diurnally varying SST in the upper-ocean skin layer on TC intensity prediction. Previous study recently reported that sea-surface skin temperature variations may affect maximum hourly precipitation over the western Pacific in boreal summer and in the seasonal climatology . However, the impact of diurnally varying SST on TC intensity prediction on a weather-forecasting time scale is not well understood. Moreover, the sensitivity of diurnally varying SST to oceanic preexisting conditions and to cumulus parameterization should be considered. Determination of whether oceanic preexisting conditions or sea-surface skin temperature variations significantly affect TC intensity prediction on a weather-forecasting time scale is, however, beyond the scope of this study.
4.2. Upper-Ocean Variability on Seasonal to Climate Scales
Here, we discuss the relationship between TC intensity prediction on a weather-forecasting time scale and upper-ocean variability on seasonal to climate time scales. Even though the time scales are different, initial oceanic conditions for predicting Hai-Tang can indeed be determined by analysis of the oceanic field, including oceanic variations on both weather-forecasting and seasonal to climate time scales. Wada and Chan  investigate upper-ocean variability in the North Pacific on seasonal to climate time scales in the North Pacific by using monthly oceanic reanalysis data sets calculated by MOVE. Table 3 lists the correlation coefficients between the nine NHM and NCM predicted central pressures at 72 h and the normalized amplitudes in July from 1997 to 2005. Wada and Chan  already derived the normalized amplitudes by Empirical Orthogonal Function analysis (EOF) of the 44-year monthly North Pacific TCHP data set. The central pressures predicted by the NCM at 72 h were significantly correlated with the normalized amplitudes of EOF first mode (EOF1) at a 90% significance level (Table 3), indicating a significant relationship between predicted central pressures at 72 h around N, E, and ENSO events . In contrast, central pressures predicted by the NHM were significantly correlated with the normalized amplitudes of EOF second mode (EOF2) at the 80% significance level. In fact, the region with remarkable SSC around Hai-Tang’s predicted track corresponds to that where TCHP remained high. The high TCHP is associated with ENSO Modoki event, when all of the North Pacific except its eastern tropical part was relatively warm . In contrast, the region with remarkable SSC corresponds to that where TCHP decreased owing to the passage of the TC during El Niño. Conversely, predicted central pressure was lowest in 1999 during the transition to a mature La Niña event, implying that a climatologically deep mixed layer in the WNP during La Niña events may cause TCs to intensify.
Chia and Ropelewski  reported that the climatological mean location of TC formation varies in relation to ENSO. In that sense, certain oceanic preexisting conditions matched the certain atmospheric conditions to produce reasonable atmospheric and oceanic environmental fields, which are necessary for tropical cyclogenesis and intensification in the case of super-typhoon Hai-Tang. In other words, the atmospheric thermodynamics conditions favorable to tropical cyclogenesis and intensification are associated with the oceanic preexisting conditions. Here we take as an example a typhoon generated in July 2004 in the area where Hai-Tang was generated and intensified in 2005. A tropical storm was generated at around N, E at 0600 UTC on 11 July 2004, and it became a tropical cyclone, named Typhoon Kompasu, at 0000 UTC on 14 July 2004 in a location near Hai-Tang’s track. The minimum central pressure of Kompasu was 992 hPa. Thus, Kompasu did not show remarkable intensification in 2004 even though in 2005 Hai-Tang was generated and intensified in the same location. Oceanic preexisting conditions in 2004 led to the weak intensity of Kompasu, consistent with the weak intensity of predicted Hai-Tang under the initial oceanic conditions of 12 July 2004 (Figures 3(a) and 3(b)). Thus, certain large-scale atmospheric forcing must accompany the certain oceanic preexisting conditions to cause the tropical cyclogenesis and intensification of a super-typhoon such as Hai-Tang.
We qualitatively evaluated the impact of variations in oceanic preexisting conditions on predictions of Typhoon Hai-Tang in 2005 by a coupled atmosphere-ocean model to which we provided nine initial oceanic conditions obtained from daily oceanic reanalysis data for 12 July from 1997 to 2005. Our conclusions are as follows.(1)The amplitude of the impact of the variations in oceanic preexisting conditions on predicted Hai-Tang’s central pressure was nearly 18 hPa at 72 h, compared with a predicted central pressure difference of about 40 hPa at 72 h, predicted from the difference in sea-surface temperature (SST) between the nonhydrostatic atmospheric model (NHM) and the nonhydrostatic atmosphere model coupled with the ocean model (NCM). The marked difference between the predicted SST and the initial SST is the sea-surface cooling (SSC) caused by the passage of Hai-Tang. The impact of SSC was more remarkable than that of variations in oceanic preexisting conditions on Hai-Tang’s intensity prediction. However, to evaluate the impact of the variation in oceanic preexisting conditions on predicted Hai-Tang’s central pressure quantitatively, the effect of cumulus parameterization should be considered. Numerical-prediction experiments with NCM at horizontal resolutions of 1-2 km will be needed in the future because of the poor intensity prediction by even the NHM at the 6-km horizontal resolution.(2)Warm-core oceanic eddies and a climatologically deep mixed layer led to a high mixed-layer heat potential, which increased the latent heat flux and enhanced the water vapor and liquid water contents, leading to increases in Hai-Tang’s atmospheric warm-core temperature owing to latent heat release and thus intensification of Hai-Tang. The difference in the intensity predictions of Hai-Tang among the nine NCM predictions accompanied that in the hourly changes in potential temperature caused by radiation. Variations in oceanic preexisting conditions were sensitive to precipitation intensities along the spiral rainbands and thus affected Hai-Tang’s intensity, whereas SSC negatively affected the formation of an axisymmetric precipitation pattern near Hai-Tang’s center.
We discussed the requirement that certain large-scale atmospheric forcing must accompany the certain oceanic preexisting conditions to cause the tropical cyclogenesis and intensification of a super-typhoon such as Hai-Tang. Chan  also reported that locations of TC genesis varied depending on the atmospheric dynamic forcing. However, it is not well understood how the atmospheric thermodynamic field and associated oceanic preexisting conditions affect TC intensity. In this study, we successfully evaluated uncertainties in predictions of Hai-Tang’s intensity related to variations in oceanic preexisting conditions. This is the first step to understanding the impact of the atmospheric thermodynamic field and its associated oceanic preexisting conditions on TC intensity and to making TC intensity prediction more precise. To explore this further, a more sophisticated oceanic data assimilation system and coupled atmosphere(-wave)-ocean model are needed. In addition, the results of the coupled model suggest that we should consider seasonal to climate variations in oceanic conditions to improve the intensity predictions on a weather-forecasting scale.
A. Wada is grateful to Dr. Y. Kawai for developing the oceanic sublayer scheme. This work was supported by the Japan Society for the Promotion of Science (JSPS), Grant-in-Aid for Scientific Research (C) (19612005 and 22540454). The authors thank Dr. T. Kato of the Meteorological Research Institute, Japan Meteorological Agency, for the use of his plotting tools. General Mapping Tools (GMT) were also used to draw figures.
- Z.-W. Zheng, C.-R. Ho, and N.-J. Kuo, “Importance of pre-existing oceanic conditions to upper ocean response induced by Super Typhoon Hai-Tang,” Geophysical Research Letters, vol. 35, no. 20, Article ID L20603, 2008.
- A. Wada, H. Niino, and H. Nakano, “Roles of vertical turbulent mixing in the ocean response to Typhoon Rex (1998),” Journal of Oceanography, vol. 65, no. 3, pp. 373–396, 2009.
- A. Wada, K. Sato, N. Usui, and Y. Kawai, “Comment on “Importance of pre-existing oceanic conditions to upper ocean response induced by Super Typhoon Hai-Tang” by Z.-W. Zheng, C.-R. Ho, and N.-J. Kuo,” Geophysical Research Letters, vol. 36, no. 9, Article ID L09603, 2009.
- C.-R. Ho, Q. Zheng, Z.-W. Zheng, N.-J. Kuo, C.-K. Tai, and F.-C. Su, “Reply to comment by A. Wada et al. on “Importance of pre-existing oceanic conditions to upper ocean response induced by Super Typhoon Hai-Tang”,” Geophysical Research Letters, vol. 36, no. 9, Article ID L09604, 2009.
- A. Wada, “Numerical problems associated with tropical cyclone intensity prediction using a sophisticated coupled typhoon-ocean model,” Papers in Meteorology and Geophysics, vol. 58, pp. 103–126, 2007.
- A. Wada and N. Usui, “Importance of tropical cyclone heat potential for tropical cyclone intensity and intensification in the Western North Pacific,” Journal of Oceanography, vol. 63, no. 3, pp. 427–447, 2007.
- A. Wada and J. C. L. Chan, “Relationship between typhoon activity and upper ocean heat content,” Geophysical Research Letters, vol. 35, no. 17, Article ID L17603, 2008.
- A. Wada, “Idealized numerical experiments associated with the intensity and rapid intensification of stationary tropical-cyclone-like vortex and its relation to initial sea-surface temperature and vortex-induced sea-surface cooling,” Journal of Geophysical Research, vol. 114, no. 18, Article ID D18111, 2009.
- I. Ginis, “Ocean response to tropical cyclone,” in Global Perspective on Tropical Cyclones, R. L. Elsberry, Ed., pp. 198–260, WMO/TD-No. 693, Geneva, Switzerland, 1995.
- N. Usui, S. Ishizaki, Y. Fujii, H. Tsujino, T. Yasuda, and M. Kamachi, “Meteorological Research Institute multivariate ocean variational estimation (MOVE) system: some early results,” Advances in Space Research, vol. 37, no. 4, pp. 806–822, 2006.
- K. Saito, T. Fujita, Y. Yamada et al., “The operational JMA nonhydrostatic mesoscale model,” Monthly Weather Review, vol. 134, no. 4, pp. 1266–1298, 2006.
- A. Wada and Y. Kawai, “The development of diurnally-varying sea-surface temperature scheme. Part I. Preliminary numerical experiments,” CAS/JSC WGNE, Research Activities in Atmospheric and Ocean Modelling, vol. 39, no. 4, pp. 0907–0908, 2009.
- Y.-L. Lin, R. D. Farley, and H. D. Orville, “Bulk parameterization of the snow field in a cloud model,” Journal of Climate & Applied Meteorology, vol. 22, no. 6, pp. 1065–1092, 1983.
- J. S. Kain and J. M. Fritsch, “A one-dimensional entraining/detraining plume model and its application in convective parameterization,” Journal of the Atmospheric Sciences, vol. 47, no. 23, pp. 2784–2802, 1990.
- J. Kondo, “Air-sea bulk transfer coefficients in diabatic conditions,” Boundary-Layer Meteorology, vol. 9, no. 1, pp. 91–112, 1975.
- J. B. Klemp and R. Wilhelmson, “The simulation of three-dimensional convective storm dynamics,” Journal of the Atmospheric Sciences, vol. 35, pp. 1070–1096, 1978.
- J. W. Deardorff, “Stratocumulus-capped mixed layers derived from a three-dimensional model,” Boundary-Layer Meteorology, vol. 18, no. 4, pp. 495–527, 1980.
- M. Sugi, K. Kuma, and K. Tada, “Description and performance of the JMA operational global spectral model (JMA-GSM88),” Geophysical Magazine, vol. 43, pp. 105–130, 1990.
- A. Schiller and J. S. Godfrey, “A diagnostic model of the diurnal cycle of sea surface temperature for use in coupled ocean-atmosphere models,” Journal of Geophysical Research, vol. 110, no. 11, Article ID C11014, 2005.
- J. C. Ohlmann and D. A. Siegel, “Ocean radiant heating. Part II: parameterizing solar radiation transmission through the upper ocean,” Journal of Physical Oceanography, vol. 30, no. 8, pp. 1849–1865, 2000.
- M. A. Brunke, X. Zeng, V. Misra, and A. Beljaars, “Integration of a prognostic sea surface skin temperature scheme into weather and climate models,” Journal of Geophysical Research, vol. 113, no. 21, Article ID D21117, 2008.
- H. H. Chia and C. F. Ropelewski, “The interannual variability in the genesis location of tropical cyclones in the northwest Pacific,” Journal of Climate, vol. 15, no. 20, pp. 2934–2944, 2002.
- J. C. L. Chan, “Thermodynamic control on the climate of intense tropical cyclones,” Proceedings of the Royal Society A, vol. 465, no. 2110, pp. 3011–3021, 2009.