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Transmission of the electric fields to the low latitude ionosphere in the magnetosphere-ionosphere current circuit
Geoscience Letters volume 3, Article number: 4 (2016)
The solar wind energy is transmitted to low latitude ionosphere in a current circuit from a dynamo in the magnetosphere to the equatorial ionosphere via the polar ionosphere. During the substorm growth phase and storm main phase, the dawn-to-dusk convection electric field is intensified by the southward interplanetary magnetic field (IMF), driving the ionospheric DP2 currents composed of two-cell Hall current vortices in high latitudes and Pedersen currents amplified at the dayside equator (EEJ). The EEJ-Region-1 field-aligned current (R1 FAC) circuit is completed via the Pedersen currents in midlatitude. On the other hand, the shielding electric field and the Region-2 FACs develop in the inner magnetosphere, tending to cancel the convection electric field at the mid-equatorial latitudes. The shielding often causes overshielding when the convection electric field reduces substantially and the EEJ is overcome by the counter electrojet (CEJ), leading to that even the quasi-periodic DP2 fluctuations are contributed by the overshielding as being composed of the EEJ and CEJ. The overshielding develop significantly during substorms and storms, leading to that the mid and low latitude ionosphere is under strong influence of the overshielding as well as the convection electric fields. The electric fields on the day- and night sides are in opposite direction to each other, but the electric fields in the evening are anomalously enhanced in the same direction as in the day. The evening anomaly is a unique feature of the electric potential distribution in the global ionosphere. DP2-type electric field and currents develop during the transient/short-term geomagnetic disturbances like the geomagnetic sudden commencements (SC), which appear simultaneously at high latitude and equator within the temporal resolution of 10 s. Using the SC, we can confirm that the electric potential and currents are transmitted near-instantaneously to low latitude ionosphere on both day- and night sides, which is explained by means of the light speed propagation of the TM0 mode waves in the Earth-ionosphere waveguide.
This article reviews the transmission of the electric field and currents from the dynamos in the magnetosphere down to the equatorial ionosphere to better understand the ionospheric and geomagnetic disturbances at mid and low latitudes during substorms and storms. The dynamo for the convection electric field and the Region-1 field-aligned currents (R1 FACs) is reviewed in “Convection electric field and global DP2 currents” section, and that for the shielding/overshielding and the R2 FACs in “Overshielding electric field and CEJ” section. These two kinds of electric fields and currents play a crucial role in the substorm and storm as reviewed in “DP2 and CEJ during the substorm” and “Stormtime electric field and EEJ/CEJ” sections, respectively. The geomagnetic sudden commencement is briefly reviewed in “Electric field and currents during the SC” section as an introduction to the mechanism for the near-instantaneous transmission from the polar ionosphere to the equator as reviewed in detail in “Electric field transmission mechanism” section.
Convection electric field and global DP2 currents
The magnetospheric convection is initiated by the reconnection between the southward interplanetary magnetic field (IMF) and the Earth’s magnetic field at the magnetopause (Dungey 1961). The convection electric field is generated by the dynamo around the cusp/mantle region where the solar wind energy is converted to the thermal energy of high-pressure plasma (Tanaka 1995). Figure 1 shows dynamo currents with red lines flowing (right) across the magnetic field lines (left) in the tailward cusp/mantle region and the Region-1 field-aligned currents (R1 FACs) with black lines flowing into the polar ionosphere assumed at 3.5 Re in the simulation. The red and black colors in Fig. 1 indicate negative and positive J·E (J: current, E: electric field), respectively, referring to the generation and consumption of the electromagnetic energy. The dynamo provides the dawn-to-dusk convection electric field and the R1 FACs flowing into/up from the polar ionosphere in the morning/afternoon sector, coinciding with the satellite observations (Iijima and Potemra 1976). The dawn-to-dusk electric field propagates near-instantaneously to low latitude (Kikuchi et al. 1996), directing eastward on the dayside and westward on the nightside.
The convection electric field drives the DP2 currents composed of two-cell Hall current vortices at high latitude and zonal currents at the equator (Nishida 1968). The DP2 magnetic fluctuations are well correlated with the southward IMF (Nishida 1968) and occur simultaneously at high latitude and equator (Kikuchi et al. 1996). Figure 2 shows DP2 fluctuations at high latitude (Nurmijarvi) and equator (Mokolo) with the correlation coefficient of 0.9 and no time shift greater than 25 s, suggesting near-instantaneous transmission of the convection electric field to the equator same as for the preliminary impulse (PI) of the geomagnetic sudden commencement (SC) (Araki 1977). The ionospheric currents decrease with decreasing latitude because of the geometrical attenuation, but increased at the dayside equator where the currents are intensified by the Cowling effect (EEJ) (Hirono 1952; Baker and Martyn 1953). The enhanced EEJ is an important feature of the equatorward extension of ionospheric currents from the polar ionosphere. Figure 3 shows a schematic diagram of the R1 FACs-EEJ circuit via the polar ionosphere achieved when the R1 FACs dominates over the R2 FACs under the southward IMF condition (Kikuchi et al. 1996). A current circuit is completed by the midlatitude Pedersen currents carried by the TM0 mode wave in the Earth-ionosphere waveguide (Kikuchi and Araki 1979).
It should be noted that the DP2 electric fields in the evening are significantly enhanced having the same direction as those in the day (Abdu et al. 1988). Figure 4 shows that the eastward electric field in the afternoon-evening hours (upward drift velocity indicated with the thick solid curves in Fig. 4, top) is well correlated with the DP2 currents at the dayside equator (ALCANTARA in the middle) and afternoon high latitude (NURMIJARVI in the bottom). The evening anomaly is a unique feature of the global distribution of the electric potential as calculated by the potential solver with an input of the field-aligned currents in the polar ionosphere (Senior and Blanc 1984; Tsunomura and Araki 1984). Figure 5 shows the electric field calculated for the equator with the model of Tsunomura and Araki (1984) (T and A), Senior and Blanc (1984) (S and B) and Tsunomura (1999) (New), reproducing the evening anomaly with the same direction as in the day and enhanced magnitude.
The diurnal magnetic variation at the geomagnetic equator is often depressed substantially during disturbed periods (Matsushita and Balsley 1972). Matsushita and Balsley (1972) critically discussed that the DP2 fluctuations should be measured negative from the quiettime diurnal variation. However, the good correlation between the DP2 fluctuations at high and equatorial latitudes (Kikuchi et al. 1996) are in favor of measuring positive as was done by Nishida (1968). The depression of the diurnal variation must be caused by a westward electric field due to the disturbance dynamo (Blanc and Richmond 1980), which is activated in the midlatitude thermosphere/ionosphere by the westward thermospheric wind having traveled from the disturbed polar thermosphere.
Overshielding electric field and CEJ
The enhanced convection electric field drives an earthward motion of plasma in the plasma sheet, generating the partial ring current and Region-2 field-aligned currents (R2 FACs) in the inner magnetosphere (Vasyliunas 1972). The partial ring current builds up the shielding electric field with an opposite direction to the convection electric field, which intensifies the electric field at auroral latitude but reduces it at the mid and low latitudes. The time constant of the growth of the shielding has been estimated as 20 min from the magnetometer observations (Somayajulu et al. 1987) and 20–30 min from the theoretical calculations (Peymirat et al. 2000).
When the convection electric field reduces abruptly because of the northward turning of the IMF, the electric field reverses its direction at mid-equatorial latitudes, causing the equatorial counter electrojet (CEJ) (Rastogi 1977). The reversal of the electric field was confirmed by the Jicamarca incoherent scatter radar at the equator, which was identified as the overshielding electric field (Kelley et al. 1979; Gonzales et al. 1979).
DP2 and CEJ during the substorm
The substorm growth phase is initiated by the southward turning of the IMF, which causes the DP2 currents in the ionosphere (McPherron 1970; Kamide et al. 1996). Kikuchi et al. (2000) separated out the convection and shielding electric fields during the substorm as shown in Fig. 6 where the solid/dashed curves indicate the convection/shielding electric fields at (top) auroral and (bottom) subauroral latitudes. The convection electric field dominates during the growth phase before the onset identified with the midnight Pi2 (vertical dotted line); however, the shielding electric field develops after the onset, leading to the overshielding when the shielding electric field dominates over the convection electric field in the recovery of the substorm as shown in Fig. 6 (bottom). The overshielding electric field drives the equatorial CEJ, causing the equatorial enhancement of the negative bay (Kikuchi et al. 2000).
Figure 7 indicates a schematic diagram of the substorm currents composed of the partial ring current, R2 FACs, and the equatorial CEJ with the Hall currents surrounding the R2 FACs causing reversal of the ionospheric currents at midlatitude (Kikuchi et al. 2003). It is to be noted that the overshielding electric field starts to increase at the onset of the substorm and continues to grow during the expansion phase under the steady southward IMF condition (Wei et al. 2009; Hashimoto et al. 2011). Hashimoto et al. (2011) showed that both the R1 and R2 FACs develop during the substorm and that the R2 FACs is strong enough to cause overshielding. In contrast, the convection electric field was reported to be dominant during the substorm based on the analyses of the sawtooth events (Huang 2009). The contradictory observations could be due to the solar wind conditions responsible for the isolated and periodic substorms or due to the definition of the substorm whether the sawtooth events are substorms or not. If the sawtooth events were the convection bays, the electric field at low latitude would be the convection electric field same as the DP2 events. The substorm current circuits have been reproduced by the global MHD simulations, showing that the partial ring currents intensified by pressurized plasma in the near-earth magnetotail generate the R2 FACs (Tanaka et al. 2010). Furthermore, the substorm CEJ has been reproduced with the global MHD simulation, supporting the overshielding currents flowing to the equator during the substorm (Ebihara et al. 2014).
Stormtime electric field and EEJ/CEJ
The auroral electrojet expands equatorward during storms, driving the DP2 currents at midlatitudes (Feldstein et al. 1997; Wilson et al. 2001; Kikuchi et al. 2008). Wilson et al. (2001) suggested that the electric field associated with the DP2 currents might have contributed to the development of the storm ring current in the inner magnetosphere. Actually, strong convection electric fields have been observed by CRRES and Akebono at L = 2–6 (Wygant et al. 1998; Shinbori et al. 2005; Nishimura et al. 2006). The electric field is as strong as 46 mV/m during the major storm on 13 March, 1989 (Shinbori et al. 2005). The convection electric field penetrates to the equatorial ionosphere, intensifying the EEJ on the dayside (Kikuchi et al. 2008).
Rastogi (2004) demonstrated that the magnitude of the geomagnetic storm was significantly enhanced at the dayside dip equator, which was caused by the CEJ due to the northward turning of the IMF. Kikuchi et al. (2008) further showed that the geomagnetic storm was enhanced with an equatorial to low latitude amplitude ratio of 2.7 as shown in Fig. 8 where the storm at low latitude (OKI) is caused by the ring current but those at the equator (GAM, YAP) is significantly enhanced by the EEJ. The EEJ derived as a difference between the disturbances at the low latitude and equator is intensified during the main phase (02-04UT, Fig. 9, bottom), while the CEJ develops during the recovery phase (04-06 UT). Both the EEJ and CEJ contribute to the equatorial enhancement of the geomagnetic storm. The recovery phase CEJ was shown to be associated with the rapid poleward shift of the auroral electrojet as shown with the contours of the ionospheric current intensity in Fig. 9 (top), suggesting that the stormtime CEJ may have been caused by substorms. It is to be noted that the shielding became effective in late main phase and overshielding occurred during the recovery phase in contrast to that Huang et al. (2005) pointed out that the convection electric field continued to penetrate to low latitude for many hours during the storm. The time constant of the overshielding still remains a crucial issue, since the direction of the electric field at midlatitude would play a key role in the generation/decay of the equatorial ionospheric anomaly, magnetic disturbances, and probably ring current development/decay in the inner magnetosphere. Indeed, the overshielding electric field has been detected by the CRRES and Akebono satellites in the inner magnetosphere during the recovery phase (Wygant et al. 1998; Nishimura et al. 2006), which would contribute to the decay of the ring current.
The stormtime current circuits are composed of the R1 FAC-EEJ during the main phase and the R2 FAC-CEJ during the recovery phase, which are similar to those of the substorm growth and expansion phases, respectively. It should be noted, however, that the CEJ occurs even during the storm main phase (Fejer et al. 2007), which could have been caused by the disturbance dynamo activated by the preceding storm activities. It should be reminded that the disturbance dynamo begins to work with a time lag of several hours from the beginning of storm and continues to work for, say, 10 h (Fejer and Scherliess 1997). In contrast, the overshielding develops quickly responding to the solar wind conditions and substorm activities. The latitude and local time distribution of the ionospheric electric field would enable us to distinguish the overshielding from the disturbance dynamo.
Electric field and currents during the SC
The ionospheric currents achieved during the geomagnetic sudden commencement (SC) are similar to the DP2 currents except that the time scale of the SC is as short as a few minutes or even less. The SC is composed of the preliminary impulse (PI) and main impulse (MI) superimposed on the stepwise increase (DL) (Araki 1994). The PI and MI with typical time scales of 1 and 5 min are caused by the ionospheric currents driven by the dusk-to-dawn and dawn-to-dusk electric fields, respectively. The DL is caused by the compressional MHD waves launched by the intensified magnetopause currents (Tamao 1964). Both the PI and MI are characterized by the equatorial enhancement (Araki 1994) and the electric fields on the day- and night sides are opposite to each other except that the electric fields in the evening are in the same direction as in the day (Kikuchi 1986). The evening anomaly of the PI and MI electric fields leads to the fact that they are potential fields transmitted with the ionospheric currents, similar to the convection electric fields.
Electric field transmission mechanism
Using the SC, we can confirm the simultaneous occurrence at high latitude and equator within the temporal resolution of 10 s. Araki (1977) found that the PI started simultaneously at the equator (KO in Fig. 10) and high latitude (PB, CO, SI) and suggested that the equatorial PI is caused by the polar electric field having propagated to the equator instantaneously. The instantaneous transmission of the polar electric field was explained by means of the TM0 mode electromagnetic waves propagating at the speed of light in the Earth-ionosphere waveguide (Kikuchi and Araki 1979). The TM0 mode is equivalent to the TEM (transverse electromagnetic) mode in the two-conductor transmission line. As seen in Fig. 10, the equatorial PI looks isolated from the high latitude PI. This is because the propagation of the electric field suffers severe geometrical attenuation (Kikuchi and Araki, 1979) and no or small PI is observed at mid and low latitudes (FR, TU, HO). Figure 11 shows a schematic diagram of the three-layered Earth-ionosphere waveguide terminated by the fully ionized magnetosphere (Kikuchi 2014). The positive electric potential (+V 0) is transmitted with the downward FAC (thick arrow) to the left end of the waveguide, providing the vertical electric field, E zV in the waveguide, which excites the TM0 mode wave propagating with the horizontal Poynting flux, S xV, at the speed of light. The TM0 mode wave carries electric currents in the ionosphere and on the ground, which are connected by the displacement current on the wave front of the TM0 mode wave. The same propagation mechanism works for the negative potential of the upward FAC. Then, a current circuit is completed between the magnetospheric dynamo and the equatorial ionosphere as schematically shown in Fig. 12, which allows the dynamo current to flow into the global ionosphere and further into the ground even in a steady state. Under an assumption of an east–west symmetry, the positive and negative potentials meet and cancel each other in the noon-midnight meridian. The ionosphere with zero-potential is effectively connected to the ground with zero-potential. Thus, the noon-midnight meridian can be replaced with a perfectly conducting sheet as shown with the vertical dashed line at noon, on which downward and upward currents of the same amount are supposed to take part in the duskside and dawnside current circuits driven by the positive and negative potentials, respectively. Replacing the waveguide with the finite-length parallel plane transmission line, Kikuchi (2014) calculated the electric potential and currents in the ionosphere and showed that the ionospheric currents grow to the steady-state value with the time constant of a few to 10s of seconds, depending on the ionospheric conductivity. The transmission line model well explains the instantaneous onset of the PI at all latitudes and delayed peak at the equator by 20 s (Takahashi et al. 2015). The global distribution of the steady-state currents is readily calculated using the potential solver (Tsunomura and Araki 1984).
Since the TM0 mode wave has no low cutoff frequency, the propagation suffers no attenuation at all frequencies (Budden 1961). However, the TM0 mode waves suffer geometrical attenuation causing the intensity at low latitude to be less than 10 percent of the source field (Kikuchi and Araki 1979). Because of the geometrical attenuation, the ionospheric currents depending on the ionospheric conductivity are too weak to cause the PI at low latitude (Fig. 10). However, the electric field is strong enough to be detected by the HF Doppler sounder (Kikuchi 1986). The electric field associated with the ionospheric currents is transmitted by the Alfven wave upward into the F-region ionosphere and the inner magnetosphere (Kikuchi 2014), which leads to the coherent variations of the ground magnetic field and ionospheric motion at the geomagnetic equator, as observed by the HF Doppler sounders (Abdu et al. 1988) and by the Jicamarca incoherent scatter radar (Kikuchi et al. 2003). The upward transmission of the Poynting flux into the inner magnetosphere has been observed by the satellites (Nishimura et al. 2010), causing the quick development of the electric field in the inner magnetosphere (Nishimura et al. 2009), ring current (Hashimoto et al. 2002), and so on.
The convection electric field is transmitted by the Alfven wave from the dynamo in the outer magnetosphere to the polar ionosphere, accompanying the R1 FACs and driving the DP2 currents composed of ionospheric Hall currents at high latitude and the Pedersen currents amplified by the Cowling effect at the dip equator. The convection electric field is transmitted to low latitude near-instantaneously by the TM0 mode waves in the Earth-ionosphere waveguide, resulting in high correlation of the DP2 fluctuations between high latitudes and equator during storm and substorms. The electric field associated with the DP2 currents is transmitted into the F-region ionosphere and into the inner magnetosphere, causing quick response of the low latitude ionosphere and ring current development when the cross polar cap potential increases. The overshielding electric field together with the R2 FACs causes reversal of the ionospheric electric field at midlatitude and the counter electrojet at the equator during substorm expansion phase and storm recovery phase. The same current circuit is achieved in the ionosphere during the geomagnetic sudden commencements, attesting the instantaneous transmission of the electric field and currents from the polar ionosphere to the equator. The evening anomaly of the electric field directing in the same direction as in the day and enhanced magnitude is a unique feature of the electric potential in the global ionosphere, which is commonly observed during the DP2 and SC events.
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The author, TK wrote the whole manuscript with his knowledge and experience on the convection electric field and its transmission mechanism. The coauthor, KH provided the author with knowledge about the substorm over-shielding based on her experience in this specific field. The selection and preparation of the figures are also due to coauthors efforts. Both authors read and approved the final manuscript.
We would like to thank T. Araki at Geophysical Institute, Kyoto University, T. Tanaka at Kyushu University, S. Fujita at Meteorological College, Y. Omura, Y. Ebihara and A. Shinbori at Research Institute for Sustainable Humanosphere, Kyoto University, Y. Nishimura at Department of Atmospheric and Oceanic Sciences, University of California, Los Angeles, and B. Veenadhari at Indian Institute of Geomagnetism for fruitful discussion on the electric field and magnetic field in the magnetosphere and ionosphere. The works of TK and KH are supported by the JSPS KAKENHI Grant Number 26400481 (KH) and the joint research programs of the National Institute of Polar Research, Tokyo. The study of TK is supported by the Grants-in-Aid for Scientific Research (15H05815) of Japan Society for the Promotion of Science (JSPS) and the joint research programs of the Institute for Space-Earth Environmental Research, Nagoya University, and the Research Institute for Sustainable Humanosphere, Kyoto University.
The authors declare that they have no competing interests.