Oceanic Kelvin waves: The next polar vortex*
*Okay, maybe not.
While not as popular as “polar vortex,” oceanic Kelvin waves did break into media reports in early 2014 (here, here, here) when a really strong wave traveled eastward across the tropical Pacific Ocean. In this post, we’ll go into a little more detail on what these waves are and why they are important in ENSO prediction. And if Kelvin waves ever get as popular as the polar vortex some day, we are confident our readers will be able to describe them in a way that doesn’t generate a heavy sigh from scientists.
Not all waves curl and crash
The waves that most of us are familiar with are the waves at the beach—waves that endlessly curl and crash on the shore. But the ocean and atmosphere also have what are called “planetary waves”—waves of immense scale. Kelvin waves are a kind of planetary wave.
Unlike the waves you see at the beach, Kelvin waves do not curl over and then crash. They are more like the waves in your bathtub, which slowly slosh around. They don’t break, but they still have broad peaks and valleys that change the depth of the water (the ocean equivalent is “sea surface height”).
The Kelvin waves that are relevant to ENSO only move eastward and along the equator (1). Like all planetary waves, the geographic extent of an equatorial Kelvin wave is huge, often stretching over much of the Pacific Ocean (thousands of miles).
Equatorial Kelvin waves have two phases, which can lead to very different changes in subsurface and sea surface temperature (SSTs) in the eastern tropical Pacific:
(A) Downwelling phase: Normally, winds blow from east to west across the tropical Pacific, which piles up warm water in the western Pacific. A weakening of these winds starts the surface layer of water cascading eastward. The thick warm layer sloshes east, pushing down the thermocline as it goes, thus we call this a “downwelling” wave. The thermocline is the boundary between the warmer, near surface mixed layer and colder deeper water (4). Because of this downward push as the wave travels eastward, it is harder for the colder, deeper water to affect the surface so near-surface temperatures are often above average. This will often (not always) warm the surface temperatures and plant the seeds for an El Niño (5).
(B) Upwelling phase: After the downwelling part of the wave goes by, we sometimes see a rebound or upwelling where there was once downwelling (6). Here, the colder water at depth upwells and the thermocline comes closer to the surface. We often will see below average temperatures near or at the surface.
You can see both downwelling and upwelling phases in this diagram below, which shows the average temperature of the top 300m of the ocean along the equator (7). When the warm upper layer is thick, this average temperature is warmer, so this kind of diagram is convenient. After it gets started, a Kelvin wave takes 2-3 months to cross the tropical Pacific, which gives us some lead time to anticipate a possible El Niño event. We saw a big downwelling Kelvin wave in March/April 2014 (also see this article), but then we saw an upwelling phase go through in June/July, which helped to reverse and cool temperatures in the eastern Pacific. The subsurface temperature changes are not always perfectly equal and opposite. Just because there is a strong downwelling phase does not mean there will be a strong upwelling phase (6).
During December 2014 and January 2015, we saw a weak upwelling Kelvin wave move across the tropical Pacific (white shading), which resulted in cooling of the subsurface tropical Pacific ocean. Will this be the final nail in the coffin for El Niño in winter of 2014-15? It is possible, so stay tuned to future ENSO updates. Going forward, we still need to continue to monitor the Pacific for future downwelling Kelvin waves which may increase the risk of El Niño forming in 2015 (see latest NCEP CFSv2 run).
-- Thanks for the review and edits from William Kessler, NOAA Pacific Marine Environmental Laboratory (PMEL). Check out his helpful and entertaining ENSO FAQs.
(1) At this point, our more inquisitive readers might ask themselves, what happens after this wave hits the coast of South America? Well, they can bounce back (slightly off the equator) as a westward moving Rossby wave. Also, there is a second type of Kelvin wave in the ocean that is not as directly applicable to ENSO prediction, which is called a coastal Kelvin wave that travels with the coast to its right in the Northern Hemisphere.
(2) At planetary scales, different forces dominate, and so we find these different classes of waves. However, like any wave, planetary waves begin when the surface of a fluid is disturbed somehow.
(3) The atmospheric Kelvin wave is often presented as Convectively Coupled Kelvin wave (CCKW) and is essentially similar to the atmospheric Madden Julian Oscillation (MJO) except they move faster eastward and span shorter wave lengths (Kiladis et al., 2009).
(4) The thermocline is often defined by subsurface temperatures at 20°C. Around the 20°C layer, ocean temperatures change rapidly (a strong temperature gradient). On average, the thermocline is found at a deeper depth in the western Pacific and is closer to the surface in the eastern Pacific.
(5) The appearance of a downwelling Kelvin wave does not automatically mean an El Niño event is coming. Sub-surface temperatures can get quite warm, but they do not necessarily manifest themselves at the surface of the ocean in a 1:1 fashion. This is because it is “easier” to achieve large anomalies near the thermocline (a large temperature gradient can lead to big anomalies) and not necessarily right at the surface. However, downwelling Kelvin waves are one sign of a possible El Niño and are why it is important to monitor below the surface of the ocean in addition to the surface.
(6) There does not have to be a rebound upwelling wave. The waves entirely reflect the wind forcing: if the winds remain westerly, there will be no rebound. But it happens that typically westerly wind forcing (e.g. say from the MJO) is then followed by easterly anomalies. This process is entirely external to the ocean— ultimately, the ocean will respond to sustained wind forcing.
(7) Figure 1 is referred to as a Hovmoller diagram, which is an intimidating name, but it is a nice way to present information. The red shading is showing where the subsurface temperatures (from the ocean surface to 300 meters below the surface) are above average. Blues show you where they are below average. The nice thing about this diagram is that you can see the evolution and movement of these waves over time. The upper-left to lower-right tilt of the temperature anomalies indicates eastward movement which is a sign of an oceanic Kelvin wave. In contrast, you cannot see this movement when you examine a figure simply showing the subsurface ocean temperatures at one point in time (like the one below that is for 13 January 2015). In a Hovmoller diagram, one of the axes (usually the vertical/y-axis) must be time.
Kiladis, G. N., M. C. Wheeler, P. T. Haertel, K. H. Straub, and P. E. Roundy (2009), Convectively coupled equatorial waves, Rev. Geophys., 47, RG2003.
Wang, B. (2003), Kelvin Waves. Encyclopedia of Meteorology. Ed. J. Holton. Academic Press. Pp. 1062-1067.
The ENSO blog is written, edited, and moderated by Michelle L’Heureux (NOAA CPC), Emily Becker and Tom DiLiberto (contractors to CPC), Anthony Barnston (IRI), and Rebecca Lindsey (contractor to NOAA CPO). Posts reflect the views of the bloggers themselves and not necessarily Climate.gov, NOAA, or Columbia University/IRI.