Being the extension of a wind-driven western boundary current, the Kuroshio Extension (KE) has long been recognized as a turbulent current system rich in large-amplitude meanders and energetic pinched-off eddies. An important feature emerging from recent satellite altimeter measurements and eddy-resolving ocean model simulations is that the KE system exhibits well-defined decadal modulations between a stable and an unstable dynamic state. Here the authors show that the decadally modulating KE dynamic state can be effectively defined by the sea surface height (SSH) anomalies in the 31°–36°N, 140°–165°E region. By utilizing the SSH-based KE index from 1977 to 2012, they demonstrate that the time-varying KE dynamic state can be predicted at lead times of up to ~6 yr. This long-term predictability rests on two dynamic processes: 1) the oceanic adjustment is via baroclinic Rossby waves that carry interior wind-forced anomalies westward into the KE region and 2) the low-frequency KE variability influences the extratropical storm tracks and surface wind stress curl field across the North Pacific basin. By shifting poleward (equatorward) the storm tracks and the large-scale wind stress curl pattern during its stable (unstable) dynamic state, the KE variability induces a delayed negative feedback that can enhance the predictable SSH variance on the decadal time scales.
The Kuroshio Extension (KE) is an eastward-flowing, inertial jet in the subtropical western North Pacific Ocean after the Kuroshio separates from the coast of Japan. Being the extension of a wind-driven western boundary current, the KE has long been recognized as a turbulent current system rich in large-amplitude meanders and energetic pinched-off eddies (e.g., Mizuno and White 1983; Qiu and Chen 2005; Kelly et al. 2010). Not only is it a region abundant with oceanic mesoscale variability, the KE region is also where the largest interannual and longer time scale ocean circulation changes are detected in the North Pacific Ocean (Fig. 1a).
A significant advancement has been made over the last decade regarding the phenomenology and the dynamic causes for the low-frequency KE changes based on satellite altimeter measurements and eddy-resolving ocean general circulation models (OGCMs). It is by now well established that the KE system exhibits clearly defined decadal modulations between a stable and an unstable dynamic state (e.g., Qiu and Chen 2005, 2010; Taguchi et al. 2007, 2010; Kelly et al. 2007; Ceballos et al. 2009). When in its stable dynamic state, the KE jet tends to have an intensified eastward transport, a northward latitudinal position, an enhanced southern recirculation gyre, and a decreased regional eddy kinetic energy level. The reverse is true when the KE jet switches to an unstable dynamic state.
What is responsible for the transitions between the stable and unstable states of the KE system has been explored extensively both observationally and based on ocean circulation models of various complexities (Miller et al. 1998; Seager et al. 2001; Schneider et al. 2002; Qiu 2003; Taguchi et al. 2007; Sasaki et al. 2013). The consensus reached by these studies is that the transitions are controlled by the decadally fluctuating wind stress curl forcing over the central midlatitude North Pacific Ocean. Specifically, when the central North Pacific wind stress curl anomalies are positive, enhanced Ekman flux divergence generates negative local sea surface height (SSH) anomalies. As these wind-induced negative SSH anomalies propagate westward into the KE region after a delay of 3–4 yr, they weaken the zonal KE jet, leading to an unstable state of the KE system with a reduced recirculation gyre and an active eddy kinetic energy field. The negative, anomalous wind stress curl forcing in the central North Pacific, on the other hand, generates positive SSH anomalies through the Ekman flux convergence. After propagating into the KE region in the west, these anomalies stabilize the KE system by increasing the KE transport and shifting its position northward.
The decadally modulating KE dynamic state brings about significant changes in the regional sea surface temperature, upper-ocean heat content, and water mass properties of subtropical mode water, central mode water, and North Pacific Intermediate Water (Qiu 2000; Vivier et al. 2002; Qiu and Chen 2006, 2011; Oka et al. 2012). For example, the elevated eddy variability during the KE unstable state brings upper-ocean high potential vorticity water of the mixed water region southward, creating a stratified upper-ocean condition in the southern recirculation gyre region unfavorable for the wintertime deep convection and subtropical mode water formation. By affecting the regional thermal conditions and mesoscale eddy activities, the decadal KE variability has also been found to exert a great influence on marine ecosystems and fisheries in the western North Pacific Ocean (e.g., Noto and Yasuda 1999; Miller et al. 2004; Nishikawa et al. 2011).
With such broad impacts, it is natural to inquire if the dynamic state of the KE system can be predicted into the future. Given the delayed adjustment by the KE jet in response to the surface wind stress forcing, the westward propagation process has been exploited in the past in predicting the wintertime sea surface temperature (SST) anomalies north of the KE jet by Schneider and Miller (2001) and the KE jet speed by Nonaka et al. (2012). Note that, in these “one way” prediction studies, the predicted KE dynamic state is determined entirely by the adopted ocean model dynamics and has no dependency on future wind variability.
The objective of our current study is to explore the extent to which we may extend the prediction of the KE dynamic state by taking into account the ocean–atmosphere coupling between the KE and overlying atmosphere. By transporting warmer tropical water poleward to the midlatitude North Pacific, the KE provides a significant source of heat and moisture for the overlying atmosphere (Fig. 1b). This source of oceanic origin has been demonstrated by several recent studies to help maintain the lower tropospheric baroclinicity and anchor the extratropical storm tracks (Fig. 1c) (Hoskins and Valdes 1990; Nakamura et al. 2004; Minobe et al. 2008; Joyce et al. 2009; Tokinaga et al. 2009; Taguchi et al. 2009; Kwon et al. 2010). Many data analysis studies in the past decade have examined the impact of the SST changes in the KE region upon the atmospheric circulation changes over the North Pacific basin (e.g., Wu et al. 2003; Frankignoul and Sennéchael 2007; Qiu et al. 2007; Frankignoul et al. 2011; Taguchi et al. 2012; Kwon and Joyce 2013). Although the KE feedback-induced atmospheric changes are weak in comparison with the internal atmospheric fluctuations (typically at 10%–15% level for the interannual and decadal signals), coupled general circulation model simulations have shown that the midlatitude air–sea coupling can enhance the decadal climate variability in the North Pacific (e.g., Latif and Barnett 1994; Pierce et al. 2001; Kwon and Deser 2007). Indeed, we will demonstrate in this study that taking into account the forcing by the KE feedback-induced surface wind anomalies can improve the long-term prediction of the dynamic state of the KE system.
The paper is organized as follows. After describing the observational data and the high-resolution OGCM product in section 2, we examine in section 3 the KE variability on decadal time scales and introduce an index that comprehensively captures the decadally fluctuating KE system. Section 4 explores how changes in the KE dynamic state affect the broad-scale surface ocean and atmosphere signals: SST, surface turbulent heat fluxes, storm track activity, and Ekman pumping velocities. Relevance of this air–sea feedback upon the prediction of the KE index is quantified in section 5. Section 6 summarizes the outcome from the present study.
2. Observational data and the OFES model output
To examine the changes in the KE dynamic state, we use the global SSH anomaly dataset compiled by the Collocte Localisation Satellites (CLS) Space Oceanographic Division of Toulouse, France. This dataset merges along-track SSH measurements from all satellite altimeter missions after October 1992 and has a 7-day temporal resolution and a 1/3° longitude Mercator spatial resolution (Ducet et al. 2000). The data period analyzed in this study extends from October 1992 to December 2012. From the SSH anomaly field h′(x, y, t), the absolute SSH field is obtained by adding the mean SSH data derived by Teague et al. (1990) to the h′(x, y, t) field.
To extend the KE index time series prior to the satellite altimeter period, we utilize the output from the multidecadal hindcast run of the OGCM for the Earth Simulator (OFES). Covering the global domain from 75°S to 75°N, the OFES model has an eddy-resolving 0.1° × 0.1° horizontal grid resolution and 54 vertical levels. The model code is based on Modular Ocean Model, version 3 (MOM3), modified for optimal performance by the Earth Simulator of Japan (Sasaki et al. 2008). The model was spun up for 50 years with monthly climatological atmospheric forcing from the National Centers for Environmental Prediction–National Center for Atmospheric Research (NCEP–NCAR) reanalysis (Kistler et al. 2001). This climatological run was followed by a 63-yr hindcast integration for the period of 1950–2012 using the NCEP–NCAR reanalysis daily-mean forcing data. In the present study, the model output from the 63-yr hindcast run is analyzed.
To relate the KE variability to those at the air–sea interface and in the overlying atmosphere, we use the monthly SST and surface turbulent (sensible and latent) heat flux data of the objectively analyzed air–sea fluxes (OAFlux) product by Yu and Weller (2007) and the daily atmospheric wind and temperature data from the NCEP–NCAR reanalysis by Kistler et al. (2001). The OAFlux datasets have 1° spatial resolution and are available from 1958 to 2012, and the NCEP–NCAR reanalysis dataset has a spatial resolution of 1.9° latitude × 1.875° longitude and spans the period of 1948–2012. To infer the storm track activities, we follow Nakamura et al. (2002) and calculate synoptic-scale (2–8 days) transient eddy temperature fluxes by using the daily wind and temperature data at the 850-hPa geopotential height from the NCEP–NCAR reanalysis. For all sea surface and atmospheric variables, we derive their monthly anomaly time series by removing the climatological monthly values.
3. Decadal KE variability and its index
As noted in the introduction, the KE system has been detected in several recent studies to oscillate between a stable and an unstable dynamic state. In this section, we will update the dynamic state of the decadally varying KE system based on the satellite altimeter observations and provide rationales for constructing an index that succinctly represents the low-frequency variations of the KE system.
A visual way to describe the decadal KE jet variability is to superimpose snapshots of the KE paths in individual years (Fig. 2). Here, the KE paths are defined by the 170-cm SSH contours in the weekly absolute SSH maps from the satellite altimeter measurements [for more details see Qiu and Chen (2005)]. In the period of the past two decades, the KE paths were relatively stable in 1993–95, 2002–05, and 2010–12 and spatially convoluted paths prevailed in 1996–2001 and 2006–09. These visual changes in the KE path stability can be quantified by evaluating the length of the KE path integrated from 140° to 153°E. As shown in Fig. 3a, the KE jet is in a stable dynamic state, if the pathlength is short, and a longer pathlength signifies an unstable dynamic state. Notice that the variability in its path stability constitutes merely one aspect of the decadally modulating KE system. When the KE jet is in a stable dynamic state, satellite altimeter measurements further reveal that its eastward surface transport tends to increase (Fig. 3b), its latitudinal position tends to migrate northward (Fig. 3c), and its southern recirculation gyre tends to strengthen (Fig. 3d). The reverse is true when the KE jet switches to an unstable dynamic state. Notice that the terminology “stable” versus “unstable” is used in this study to indicate the dynamic state of the KE system; it is not in reference to the necessary condition for instability of the KE jet.
Given the correlation among these dynamic properties of the KE system, it is useful for prediction purposes to introduce a single time series that can reflect the KE’s time-varying dynamic state comprehensively. In this study, we define the KE index by averaging the anomalies of the four time series shown in Figs. 3a–d (with the sign for the KE pathlength in Fig. 3a reversed) normalized by their respective standard deviations. The gray line in Fig. 4a shows the weekly KE index thus constructed and the black line shows the low-pass filtered KE index after removal of signals shorter than the annual period. By definition, a positive KE index signifies a stable dynamic state in which the KE jet has a steady and northerly path, an increased surface transport, and an enhanced southern recirculation gyre. An unstable dynamic state with the opposite properties is denoted by a negative KE index.
A regression analysis between the KE index and the SSH anomaly time series in the North Pacific Ocean reveals that the KE index constructed from its four dynamic properties can be favorably represented by the SSH anomaly signals in the 31°–36°N, 140°–165°E region (Fig. 4c). Indeed, the linear correlation coefficient between the low-pass filtered SSH anomaly time series averaged in 31°–36°N, 140°–165°E (Fig. 4b) and the low-pass filtered KE index in Fig. 4a is as high as r = 0.96. (Like Fig. 4a, the low-pass filter used in Fig. 4b removes the SSH signals shorter than the annual period; r = 0.84 between the original weekly time series.) Notice that the 31°–36°N, 140°–165°E region is geographically occupied by the time-mean KE jet and its southern recirculation gyre. With the KE being the inertial western boundary current jet of the subtropical gyre whose variability is closely tied to its southern recirculation gyre, it makes physical sense that its time-varying dynamic state can be represented by the SSH signals in this key region.
This result of high correlation presented in Fig. 4 is important in two respects. First, it indicates that predicting the time-varying dynamic state of the KE system is equivalent to predicting anomalous SSH signals in the 31°–36°N, 140°–165°E region that encompasses the KE jet and its southern recirculation gyre. As the large-scale SSH changes in midlatitude oceans are controlled by the linear baroclinic vorticity dynamics (see Qiu 2002, and references therein), this provides us with a dynamic framework to explore the KE index prediction. Second, while formulating the KE index of Fig. 4a based on the four dynamic properties can be labor intensive, constructing the proxy KE index of Fig. 4b using the regional SSH signals is simple and straightforward. For these two reasons, we will focus hereafter in this study on the KE index based on the SSH anomalies in 31°–36°N, 140°–165°E.
To enhance the statistical confidence in exploration of predictability, it is essential to extend the time series of the KE index for as long a period as possible. To achieve this, we utilize the multidecadal OFES hindcast run output and plot in Fig. 5a the modeled SSH anomaly time series averaged in the key region of 31°–36°N, 140°–165°E. Compared to the observed SSH signals shown in Fig. 4b, the two time series have a linear correlation coefficient r = 0.81 for the overlapping period of 1992–2012. This favorable comparison indicates that the OFES hindcast captured well the decadally modulating KE system, a result consistent with the findings of other recent studies analyzing the OFES hindcast output (Nonaka et al. 2006; Taguchi et al. 2007; Ceballos et al. 2009; Sasaki et al. 2013).
From Fig. 5a, it is clear that the decadal KE modulations similar to those detected in the recent two decades have persisted following the 1976–77 regime shift in the North Pacific climate system (e.g., Trenberth and Hurrell 1994; Mantua et al. 1997). Prior to 1976–77, the KE index inferred from the OFES output exhibited shorter and less regular fluctuations, and the SSH anomalies in the KE region were not well connected to those in the central North Pacific basin (figure not shown). In our following examinations, we lengthen the observed KE index time series of Fig. 4b by appending the OFES result before September 1992 and will focus on the prediction of the interannual KE index signals after the 1976–77 regime shift. In other words, the monthly “merged” KE index shown in Fig. 5b will serve as the predictand in the following analyses.
4. Atmospheric response to the decadal KE variability
Given that the goal of this study is to examine the importance of air–sea coupling in the prediction of the KE index, it is important to first quantify the influence of the decadal KE variability upon the physical variables at the air–sea interface and in the overlying atmosphere. Specifically, we will in this section focus on four variables: the turbulent surface heat flux, SST, lower tropospheric storm track activity, and Ekman pumping velocity. Although only the Ekman pumping velocity wEk directly affects the KE index prediction (see section 5 below), examination of the other three variables helps to present a more coherent picture as to how the atmosphere responds to the KE variability across the broad North Pacific basin.
To evaluate the impact of the KE variability, we adopt the lagged correlation analysis approach proposed by Frankignoul et al. (1998). This approach has been applied by many investigators in their respective studies on the influence of the midlatitude SST variations upon the overlying atmosphere in the North Pacific basin (Wu et al. 2003; Frankignoul and Sennéchael 2007; Qiu et al. 2007; Frankignoul et al. 2011; Taguchi et al. 2012; Kwon and Joyce 2013). The essence of the Frankignoul et al. approach is to examine the covariability of an atmospheric variable (e.g., wEk) and the KE index with a lag that is longer than the intrinsic atmospheric time scale (~2 months, Deser et al. 2007) but shorter than the persistence time scale of the KE index (estimated to be 40 months). By denoting the KE index as IKE(t) and the atmospheric variable as A(x, y, t), the lagged regression coefficient
in this case, represents the spatial response of the atmospheric variable to the time-varying KE dynamic state. In (1) angle brackets denote the ensemble average over the 432 months of 1977–2012 and the time lag is set at m = 2 months. Before calculating b(x, y), we follow the previous studies and remove by linear regression the Niño-3.4 SST anomaly signals from both the IKE(t) and A(x, y, t) time series in order to minimize the low-frequency signals teleconnected from the tropics (Alexander et al. 2002).
Figure 6a shows the b(x, y) pattern for the SST anomalies. Positive anomalies appear within the broad 30°–40°N band occupied by the KE and its eastward continuation, known as the North Pacific Current. Notice that the b(x, y) pattern in Fig. 6a is similar to Fig. 4c, the SSH pattern regressed to the KE index. This similarity indicates that the warm SST anomalies in the 30°–40°N band are controlled more by oceanic processes, that is, the strengthened KE jet and its poleward migration during the positive phase of the KE index, than by the surface heat flux forcing (Qiu 2000; Vivier et al. 2002; Kwon and Deser 2007). Indeed, the spatial pattern of the turbulent heat flux anomalies regressed to the KE index (Fig. 6b) reveals that the anomalous turbulent heat flux is mostly positive (defined in this study as from the ocean to the atmosphere) over the warm SST band. In other words, the warm SST anomalies in the 30°–40°N band are damped by the air–sea turbulent heat fluxes, rather than driven by them.
It is worth emphasizing that the warm SST anomalies seen in Fig. 6a lie underneath the mean path of the North Pacific extratropical storm tracks (recall Fig. 1c). Here, we follow Nakamura et al. (2002) and have represented the storm-track activity signals by the 2–8-day bandpass-filtered poleward eddy temperature flux data at the 850-hPa level from the NCEP–NCAR reanalysis data. Figure 6c shows the b(x, y) pattern for the storm-track activity anomalies and it exhibits a clear dipolar pattern with a dividing line oriented northeast–southwestward following the mean storm track path, or the mean wEk = 0 line (the thick black line in Fig. 6c). This dipolar pattern implies a poleward (equatorward) migration of the storm tracks when the KE index becomes positive (negative). The results shown in Figs. 6a–c are consistent with the notion that the extratropical storm tracks are anchored and energized by an oceanic front and heat release (Nakamura et al. 2004; Taguchi et al. 2009). Specifically, in its positive state when the KE jet is intensified and migrated poleward, warm SST anomalies and ocean-to-atmosphere heat release tend to expand northward, bringing about a northward shift in the overlying storm tracks.
Accompanying the KE-induced northward shift of the storm tracks is the poleward migration of the large-scale Ekman pumping velocity signals. Figure 6d, showing the spatial pattern of the wEk anomalies regressed to the KE index with a 2-month lag, reveals a band of negative Ekman pumping anomalies that follows roughly the time-mean wEk = 0 contour (thick solid line in Fig. 6d). South of these northeast–southwest-aligned negative anomalies, there exists a paralleling band of positive Ekman pumping anomalies. Given that the time-mean wEk field is tilted northeast–southwestward and has a sinusoidal spatial pattern (recall Fig. 1d), the alternately signed anomaly bands in Fig. 6d reflect that the large-scale surface wind stresses tend to migrate northward when the KE index is in its positive phase.
Notice that, within the 31°–36°N band relevant for the KE index prediction (dashed box in Fig. 6d), the wEk anomalies due to the oceanic feedback are positive (negative) in the eastern (western) basin. This feedback pattern of wEk is consistent with our previous study (Qiu et al. 2007) in which, instead of the KE index introduced in this study, we used the observed SST anomalies as an indicator for the KE variability. The tendency that a northward-migrated KE jet tends to excite positive wEk anomalies in the eastern basin of the North Pacific Ocean is similarly detected in a recent study by Frankignoul et al. (2011, see their Fig. 13c). As will be detailed in the next section, this Ekman pumping forcing due to the oceanic feedback is critical to the improved long-term prediction of the KE index.
5. One-way versus two-way predictions
The large-scale, wind-induced, SSH variability in a midlatitude ocean is governed by the long-wave linear vorticity equation:
where η is the SSH anomaly of interest, cR the long baroclinic Rossby wave speed, g the gravity constant, g′ the reduced gravity, and wEk is the anomalous Ekman pumping velocity [for references and the underlying assumptions, see Qiu (2002)]. By solving Eq. (2) as an initial value problem, we can write the solution for η as follows:
where to is the initialization time and t > to. As the KE index is constructed using the SSH anomalies in this study, Eq. (3) constitutes a useful dynamic framework to explore its predictability.
Adopting this framework, we initialize the SSH anomalies in the 31°–36°N band by using the low-pass filtered SSH anomaly data, ηm (x, t), merged from the satellite altimeter data and the OFES hindcast output (see Fig. 7). We predict the subsequent KE index under 1) the Rossby wave adjustment (one way) and 2) the Rossby wave adjustment plus wind feedback (two way) scenarios.
In the one-way prediction, wEk = 0 and the initial SSH anomalies in the 31°–36°N band are simply carried westward at the long baroclinic Rossby wave speed cR:
where both the initialization time to and the lead time of prediction τ are used as time variables for ηone-way. Once the SSH anomaly signals are obtained, the predicted KE index in this one-way case is given by
where L is the length from 140° to 165°E. Using cR = 4.2 cm s−1 from the satellite altimeter measurements, we present in Fig. 8 examples of the Ione-way(τ, to) time series predicted for a 10-yr period (magenta lines). In each plot, the prediction is initiated from July of the year indicated in the plot. For comparison, the KE index IKE(t), the predictand in this case, is shown in Fig. 8 by the black lines. With the exception of 1997, the Ione-way time series appears to track IKE(t) reasonably well, at least during the initial several years of the prediction.
Notice that the predictive skills in individual years can vary, depending on the amplitude of the initial SSH anomalies existing in the central and eastern North Pacific Ocean (cf. Fig. 7). When the amplitude is small during, for example, the period when the wind-forced SSH signals change sign, the prediction of the KE index tends to have a lowered skill. By generating the Ione-way(τ; t) time series with t stepped forward monthly from 1977 to 2012, we can quantify the overall skill of the one-way prediction by
where angle brackets denote the ensemble average over the 1977–2012 period. The magenta line in Fig. 9 shows the predictive skill Sone-way as a function of lead time τ. Reflecting the importance of Rossby wave adjustment, Sone-way greatly exceeds the skill of the damped persistence prediction1 (the black line in Fig. 9). At τ = 3 yr, the Rossby wave adjustment prediction is able to explain ~45% of the KE index variance. The one-way prediction skill, however, approaches very quickly that of the damped persistence prediction when τ > 4 yr. This is so because after 4 years, most of the initial SSH signals will have reached 140°–165°E, depleting the information of the initial SSH signals (with cR = 4.2 cm s−1, the SSH anomalies can propagate westward over a distance of 60° longitude in a 4-yr period).
In the Rossby wave adjustment plus wind feedback (two way) scenario, the predicted SSH values in the KE region of 140°–165°E feedback to the Ekman pumping field (recall Fig. 6d) and can result in additional SSH changes along the baroclinic Rossby wave paths. Using Eq. (3), we can express the two-way predicted SSH signals by
where is the b value meridionally averaged within the dashed box shown in Fig. 6d and
is the two-way predicted KE index. In the examples shown in Fig. 8, the two-way predictions are indicated by the green lines in the 10-yr lead-time windows. Compared to the magenta lines based on the one-way predictions, one can visually detect a better agreement between the green and black lines when the lead time exceeds several years.
To verify this visual comparison, we evaluate the skill of the two-way prediction using the formula similar to Eq. (6) and plot Stwo-way(τ) in Fig. 9 as the green line. While the addition of the feedback Ekman pumping forcing contributes little to the KE index prediction with the lead time <4 yr, it has a noticeable impact on forecast time longer than 4 yr. Specifically, inclusion of the feedback Ekman pumping forcing can extend the 20% predictive skill to a lead time of 6–7 yr. Notice that the 4-yr lead time marks the transition when the initial SSH signals have reached the KE region and when the feedback wind-forced SSH signals from the central/eastern North Pacific Ocean start to reach the KE region.
Following the 1976–77 climate regime shift, the Kuroshio Extension system in the North Pacific has been observed to fluctuate between stable and unstable dynamic states on the decadal time scales. Manifested by the coherent changes in its stability, axis latitude, surface transport, and strength of the southern recirculation gyre, the dynamic state of the decadally varying KE system can be well represented by the SSH anomaly signals in the 31°–36°N, 140°–165°E region occupied by the time-mean KE jet and its southern recirculation gyre. Positive (negative) SSH anomalies in this region correspond to a stable (unstable) dynamic state and are defined by a positive (negative) KE index in this study. By combining the SSH anomaly signals from the satellite altimeter measurements and the eddy-resolving OFES hindcast simulation, we constructed the KE index for the period of 1977–2012.
Using the KE index thus constructed as the predictand, we explored its predictability by adopting two approaches. The first approach takes advantage of the facts that the SSH adjustment in the midlatitude ocean is via baroclinic Rossby waves and that the low-frequency wind forcing in the North Pacific has its center of action in the eastern part of the basin (Qiu 2003). With the phase speed cR = 4.2 cm s−1 by the baroclinic Rossby waves along 31°–36°N, these facts result in a delayed SSH response at the ocean’s western boundary where the KE is located. Compared to the damped persistence prediction, this “one way” prediction based on the wave adjustment process has much superior skill. Specifically, at the lead time of 4 yr, the one-way predicted KE index is able to account for 25% of the predictand’s variance, whereas the explained variance is less than 10% with the damped persistence prediction. Skill values similar to our one-way prediction have been obtained by Schneider and Miller (2001) and Nonaka et al. (2012) in their predictability studies of the SST anomalies and the KE jet speed in the western North Pacific Ocean.
In contrast to the wave adjustment approach, our second approach of exploring the KE index prediction relies on the fact that the KE jet provides a significant source of heat and moisture for the extratropical storm tracks. By modifying the paths of the storm tracks, changes in the KE dynamic state alter the basin-scale wind stress pattern, which, in turn, can feedback to the SSH field in the KE region. By utilizing the lagged regression analyses to isolate the impact by the KE variability, we found that, when the KE index is in the positive phase, the enhanced KE surface transport and its northerly position work to generate warm SST and upward turbulent heat flux anomalies along the 35°–40°N band across the North Pacific basin. These thermal forcings at the sea surface bring about the northward shift in both storm tracks and the large-scale Ekman pumping velocity field. Because the time-mean position of the wEk = 0 line in the North Pacific basin tilts northeastward from east of Japan to British Columbia, Canada, the Ekman pumping velocity induced by a stable KE system has positive anomalies in the eastern part of the 31°–36°N band. As illustrated in Fig. 10a, these positive wEk anomalies generate negative SSH anomalies in the eastern Pacific basin through the local Ekman flux divergence. As these wind-induced negative SSH signals propagate westward into the KE region, they work to switch the phase of the KE dynamic state and result in a negative KE index (Figs. 10b,c). Once the dynamic state of the KE system becomes unstable, the sequence of processes with an opposite sign shown in Fig. 10 would take place. This delayed negative feedback mechanism in the midlatitude North Pacific increases the KE variability with a preferred period of ~10 yr (Qiu et al. 2007) and is the reason behind the improved predictive skills of the KE index by this “two way” approach beyond the 4-yr lead times.
The bottom-right panel in Fig. 8 presents the decadal prediction for the future KE index based on the observed SSH anomaly data of July 2012. While both one-way and two-way predictions indicate that the KE index will remain in a positive phase (i.e., an intensified and dynamically stable state) until 2016, the two-way prediction further suggests that the KE index will transition to a negative phase (a weakened and dynamically unstable state) beyond 2017. It will be interesting to verify these predictions in the coming years based on future satellite altimeter measurements and OFES hindcast simulations.
The OFES hindcast output used in this study was provided by Dr. Hideharu Sasaki of the Earth Simulator Center, the NCEP–NCAR reanalysis data by the National Centers for Environmental Prediction, the SST and surface turbulent flux data by the WHOI OAFlux project, and the merged satellite altimeter data by the CLS Space Oceanography Division as part of the Environment and Climate EU ENACT project. We acknowledge the support of NSF OCE-0926594 and NASA NNX13AE51G to BQ and SC and of Department of Energy Grant DE-SC0005111 and DE-SC006766 to NS. BT is supported by MEXT through Grant-in-Aid for Scientific Research in Innovative Areas 2205 and JSPS through KAKENHI 24540476 and 23340139.