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factor that causes the YRB rainfall in summer. Therefore, tropical and extratropical circulation anomalies are both crucial for the YRB rainfall anomalies. The most important factor that dominates the tropical southwesterly anomalies is the zonal shift of the western North Pacific (WNP) subtropical high in the lower troposphere. The westward extension (eastward retreat) of the subtropical high corresponds to an anticyclonic (cyclonic) anomaly in the tropical WNP, and favors enhanced (suppressed
factor that causes the YRB rainfall in summer. Therefore, tropical and extratropical circulation anomalies are both crucial for the YRB rainfall anomalies. The most important factor that dominates the tropical southwesterly anomalies is the zonal shift of the western North Pacific (WNP) subtropical high in the lower troposphere. The westward extension (eastward retreat) of the subtropical high corresponds to an anticyclonic (cyclonic) anomaly in the tropical WNP, and favors enhanced (suppressed
signal is much smaller than the background climate, the important detailed information of a weather disturbance is often hidden (too weak to show) and overlooked in a conventional weather chart. In contrast, an anomaly field (i.e., a departure from climate) is found to be more directly associated with a local weather event than a full field ( Qian et al. 2016b ). This situation is illustrated by Fig. 1 , where the two “positive” events and one “negative” event are hardly visible in the full field
signal is much smaller than the background climate, the important detailed information of a weather disturbance is often hidden (too weak to show) and overlooked in a conventional weather chart. In contrast, an anomaly field (i.e., a departure from climate) is found to be more directly associated with a local weather event than a full field ( Qian et al. 2016b ). This situation is illustrated by Fig. 1 , where the two “positive” events and one “negative” event are hardly visible in the full field
1. Introduction Most of the earth’s warming signal arising from anthropogenic climate change is thought to reside in the upper ocean ( Hansen et al. 2005 ; Levitus et al. 2005 ). To understand past and present global warming trends, and so to provide data for improvement of predictions of future changes, it is necessary to refine estimates of global upper ocean heat content anomalies (OHCA) and their uncertainties. Here the effect of the irregular sampling of the world’s ocean over the last
1. Introduction Most of the earth’s warming signal arising from anthropogenic climate change is thought to reside in the upper ocean ( Hansen et al. 2005 ; Levitus et al. 2005 ). To understand past and present global warming trends, and so to provide data for improvement of predictions of future changes, it is necessary to refine estimates of global upper ocean heat content anomalies (OHCA) and their uncertainties. Here the effect of the irregular sampling of the world’s ocean over the last
transient time scale, and the temperature drop caused by a cold surge rarely persists for more than two weeks ( Zhang et al. 1997 ; Compo et al. 1999 ; Chan and Li 2004 ). In February 2008, an extreme persistent cold anomaly (ECA) accompanied by a long-persisting northerly anomaly and a sequence of cold advection occurred over Southeast Asia. The ECA persisted for nearly one month, which not only broke the lowest temperature record for the past 50 yr but also resulted in numerous agriculture and
transient time scale, and the temperature drop caused by a cold surge rarely persists for more than two weeks ( Zhang et al. 1997 ; Compo et al. 1999 ; Chan and Li 2004 ). In February 2008, an extreme persistent cold anomaly (ECA) accompanied by a long-persisting northerly anomaly and a sequence of cold advection occurred over Southeast Asia. The ECA persisted for nearly one month, which not only broke the lowest temperature record for the past 50 yr but also resulted in numerous agriculture and
Rossby wave that forms to the northwest and southwest of the heat source. These damped baroclinic Kelvin and Rossby waves depicted by the Matsuno–Gill model are the cornerstones for our understanding of heat-induced atmospheric circulations in the tropics. However, the Matuno–Gill model completely fails outside of the tropics. As demonstrated by Hoskins and Karoly (1981) and by Horel and Wallace (1981) , a diabatic heating anomaly associated with El Niño can also excite a stationary barotropic
Rossby wave that forms to the northwest and southwest of the heat source. These damped baroclinic Kelvin and Rossby waves depicted by the Matsuno–Gill model are the cornerstones for our understanding of heat-induced atmospheric circulations in the tropics. However, the Matuno–Gill model completely fails outside of the tropics. As demonstrated by Hoskins and Karoly (1981) and by Horel and Wallace (1981) , a diabatic heating anomaly associated with El Niño can also excite a stationary barotropic
( Shapiro and Keyser 1990 ). The presence of these strong horizontal PV gradients will be shown to lead to substantial changes in the structure and intensity of the balanced atmospheric response to a PV anomaly. Here and elsewhere, “balanced” refers to that portion of the time-dependent flow recoverable from PV inversion, following Davis et al. (1996) . Thorpe (1986) produced well-known diagrams of the balanced atmospheric structure associated with a circular vortex on the tropopause. Juckes (1999
( Shapiro and Keyser 1990 ). The presence of these strong horizontal PV gradients will be shown to lead to substantial changes in the structure and intensity of the balanced atmospheric response to a PV anomaly. Here and elsewhere, “balanced” refers to that portion of the time-dependent flow recoverable from PV inversion, following Davis et al. (1996) . Thorpe (1986) produced well-known diagrams of the balanced atmospheric structure associated with a circular vortex on the tropopause. Juckes (1999
-induced spicing anomalies represent the actual anomalous heat and salt transported by eddies ( Johnson and McTaggart 2010 ; Stramma et al. 2014 ; Putrasahan et al. 2015 ; Sabu et al. 2015 ), which ultimately lead to the conversion of water-mass properties ( Qiu and Chen 2011 ). Previous studies reported notable spiciness anomalies induced by mesoscale eddies. Johnson and McTaggart (2010) found Argo profiles in the east Pacific captured by subsurface anticyclonic eddies. These eddies were carrying the
-induced spicing anomalies represent the actual anomalous heat and salt transported by eddies ( Johnson and McTaggart 2010 ; Stramma et al. 2014 ; Putrasahan et al. 2015 ; Sabu et al. 2015 ), which ultimately lead to the conversion of water-mass properties ( Qiu and Chen 2011 ). Previous studies reported notable spiciness anomalies induced by mesoscale eddies. Johnson and McTaggart (2010) found Argo profiles in the east Pacific captured by subsurface anticyclonic eddies. These eddies were carrying the
1. Introduction In the 1960s and early 1970s, it was often speculated on the basis of contemporary correlations that North Pacific sea surface temperature (SST) anomalies have an influence on the large-scale atmospheric circulation on the seasonal time scale (e.g., Namias 1963 ). However, Davis (1976) showed that the cross correlation between SST and sea level pressure (SLP) anomalies reflected the atmosphere driving the ocean. This was consistent with the stochastic climate model of
1. Introduction In the 1960s and early 1970s, it was often speculated on the basis of contemporary correlations that North Pacific sea surface temperature (SST) anomalies have an influence on the large-scale atmospheric circulation on the seasonal time scale (e.g., Namias 1963 ). However, Davis (1976) showed that the cross correlation between SST and sea level pressure (SLP) anomalies reflected the atmosphere driving the ocean. This was consistent with the stochastic climate model of
1. Introduction Sea surface temperature (SST) anomalies in the Indian Ocean are characterized by a zonal dipole pattern called the Indian Ocean dipole mode ( Reverdin et al. 1986 ; Hastenrath et al. 1993 ; Harrison and Larkin 1998 ; Saji et al. 1999 ; Webster et al. 1999 ). Past studies have suggested that a possible forcing to induce the Indian Ocean dipole mode event is El Niño–Southern Oscillation (ENSO) events in the Pacific Ocean. For example, results from numerical experiments ( Lau
1. Introduction Sea surface temperature (SST) anomalies in the Indian Ocean are characterized by a zonal dipole pattern called the Indian Ocean dipole mode ( Reverdin et al. 1986 ; Hastenrath et al. 1993 ; Harrison and Larkin 1998 ; Saji et al. 1999 ; Webster et al. 1999 ). Past studies have suggested that a possible forcing to induce the Indian Ocean dipole mode event is El Niño–Southern Oscillation (ENSO) events in the Pacific Ocean. For example, results from numerical experiments ( Lau
type of event. More recently, Reynolds (1996) pointed out the similarities in the synoptic patterns for three major rainstorms during 1995. Each was associated with a strong synoptic-scale system that helped produce strong onshore flow. Pandey et al. (1999) noticed that a strong negative height anomaly to the northwest of California was associated with the 20 heaviest precipitation cases found over the Sierra Nevada during the period 1948–88. Grumm and Hart (2001a) found that significant
type of event. More recently, Reynolds (1996) pointed out the similarities in the synoptic patterns for three major rainstorms during 1995. Each was associated with a strong synoptic-scale system that helped produce strong onshore flow. Pandey et al. (1999) noticed that a strong negative height anomaly to the northwest of California was associated with the 20 heaviest precipitation cases found over the Sierra Nevada during the period 1948–88. Grumm and Hart (2001a) found that significant
