The equatorial ionization anomaly (EIA) is a prominent global-scale structuring of the terrestrial low-latitude ionosphere in the form of a trough in the F-region electron density centered on the geomagnetic (dip) equator with two peaks (crests) in the electron density on each side offset in latitude by ±15°. Originally discovered from analysis of ionosonde data (Appleton, 1946;Bailey, 1948), the EIA has been observed extensively with various ground-based and spacecraft instrumentation over many decades. It is now well-understood that EIA is formed by the combined effects of upward (vertical at the equator) E × B plasma drift and diffusion along magnetic field lines. These two forces work together to form the so-called equatorial fountain effect (e.g., Anderson, 1973;Balan et al., 2018;Hanson & Moffett, 1966;Kelley, 2009). The low-latitude E × B drift velocity is dominated by the neutral wind dynamo during geomagnetically quiet times but during active times, includes highly variable transient contributions from prompt penetration effects and longer lived effects from the disturbance dynamo (e.g., Fejer & Maute, 2021). The sensitivity of the EIA to the low-latitude E × B drift velocity (e.g., Anderson, 1973) makes it an excellent diagnostic for studying equatorial electrodynamics (e.g., Balan et al., 2009).The observed north-south asymmetry of the ionization anomaly crests with respect to the geomagnetic equator is caused by the season-dependent asymmetry in the meridional neutral winds (Anderson & Roble, 1981). Effects from the neutral atmosphere can also cause a longitudinal variation in the anomaly's occurrence and size, presumably due to the longitudinal variation of the quiet-time dynamo electric field (e.g., Fejer et al., 2008). In addition, the magnitude of the anomaly crests exhibit a 4-peak (sometimes also identified as a 3-wave) pattern in longitude for a given local time (LT), as observed by remote Far Ultraviolet (FUV) nightglow data in the evening LT sector (