International Journal of Atmospheric Sciences

Volume 2013 (2013), Article ID 130786, 9 pages

http://dx.doi.org/10.1155/2013/130786

Research Article

Concerning the Lower Atmosphere Responses to Magnetospheric Storms and Substorms

P. A. Sedykh and I. Yu. Lobycheva

Institute of Solar-Terrestrial Physics SB RAS, Lermontov Street, 126 a, P.O. Box 291, Irkutsk 664033, Russia

Received 31 January 2013; Revised 22 April 2013; Accepted 25 April 2013

Academic Editor: Helena A. Flocas

Copyright © 2013 P. A. Sedykh and I. Yu. Lobycheva. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

Abstract.

The issue of existence and physical mechanism for solar-terrestrial couplings has rather a long history. Investigations into the solar activity effect on meteorological processes in the lower atmosphere have become especially topical recently. The aim of this study is to investigate the effect of geomagnetic activity on meteorological processes in the atmosphere. We analyze the data on magnetic storms and tropical cyclones that were observed in the North Atlantic, East Pacific, and West Pacific to understand the mechanism for magnetospheric disturbance effects on complicated nonlinear system of atmospheric processes.

1. Introduction

There exist statistical correlations among geomagnetic activity, atmospheric pressure, and temperature [1–3]. Authors in [4] suggested that the observed climate response to solar variability is caused by a dynamical response in the troposphere to heating predominantly in the stratosphere.

According to [5], a tropical cyclogenesis may be “a mechanism for effective discharge of the surplus heat in the atmosphere under the conditions when the routine mechanism effect becomes insufficient.” Between the solar-terrestrial disturbance parameters, on the one hand, and the cyclogenesis characteristics, on the other, various researchers endeavor to trace hard-to-detect statistical associations. In [6], the correlation between tropical cyclones and the Cycle-23 storms was investigated. The revealed coincidence between the time of origin and evolution of the 2005 August 23-24 Hurricane Katrina with the powerful geomagnetic storm main phase [7] also boosted the research in this area.

The issue of physical mechanism for solar-terrestrial couplings has long interested researchers. Many geophysicists were almost prepared to reject the idea about a solar activity effect on the lower atmosphere condition as absolutely unacceptable. And, first of all, the matter was that the atmospheric process power enormously exceeds the solar-wind input energy flux into the near-Earth space. Due to this, it seems most unlikely that solar activity could significantly affect the lower atmosphere condition. However, the research done over the last years allowed us to find a clue to overcome this inconsistency. The main objection to a possibility of the solar activity effective influence on the lower atmosphere condition and on weather, based on insufficient power of the solar wind, appears quite surmountable; see, for example, [8]. Also, like the computations in [9] show, the energy necessary to create the atmospheric optical screen (shield) is incomparably lower than the variation amplitude in the screen-induced solar energy flux arriving at the lower atmosphere.

According to [8], variations in the atmospheric ionizing radiation flux observed during geomagnetospheric disturbances cause a noticeable variation in the chemical composition and contents of small components, as well as in the atmosphere transparency. The main types of such variations are [8] (1) galactic cosmic ray intensity short-term depressions (observed during geomagnetic disturbances (Forbush decreases)) caused by dispersion of energetic charged particles by the magnetic fields transported from the solar atmosphere by the solar wind high-velocity streams; (2) solar cosmic ray flux bursts caused by solar flares.

This paper aims to investigate geomagnetic activity effects on meteorological processes and a possible effect of magnetospheric disturbances on the tropical cyclogenesis evolution character. Usually, researchers considered magnetospheric and atmospheric problems in separate papers. This paper is an attempt to combine consistent parts taken from the meteorology ionospheric and magnetospheric physics.

2. Principal Results

A magnetospheric storm is a 1–3 day long phenomenon spanning all the magnetosphere regions, and it features sharp depressions in the magnetic field. During storms and substorms, the ionosphere undergoes rather significant Joule heating with a great power of precipitating energetic particles. Huge energy increases the ionosphere temperature and causes large-scale ion drifts and neutral winds.

We used magnetograms from ground-based stations, AE-indices, Dst-indices for each magnetospheric storm, and calculated some parameters characterizing energetic aspects of magnetospheric disturbances. The aim was to investigate a possible effect of powerful magnetospheric storms on the evolution character of meteorological processes in the atmosphere to study the correlation between magnetospheric disturbances and meteorological background variations. We also address the meteorological data for 10-day periods after these disturbances.

The power of the ionosphere’s Joule heating is either calculated through the Assimilative Mapping of Ionospheric Electrodynamics (AMIE) [10] or estimated based on empirical formulas as the AE-index function [11]: , where is in GWatt and the AE-index is in nT. The power of the energetic particles precipitating into the ionosphere can be also estimated based on empirical formulas [12]. We also used the databases for hurricanes at http://www.nhc.noaa.gov/pastall.shtml, http://www.csc.noaa.gov/hurricane_tracks, and http://www.aoml.noaa.gov/hrd/hurdat/ushurrlist18512007.txt. To study the surface pressure, the temperature, and other characteristics, we used the data at ftp://ftp.cdc.noaa.gov/. The information on tropical cyclones was obtained from http://russian.wunderground.com/hurricane/hurrarchive.asp?region=at.

The 1986 May 3 magnetospheric storm over the (0000-1100) UT interval was studied within the international CDAW9C (Coordinated Data Analysis Workshop) Project and represented a 4-substorm chain [13]. This event refers to magnetospheric storms that occurred during solar Cycle-21. It featured the AE-index reaching the values of about 1400–1500 nT, whereas the Dst-index reached only −70–80 nT (see Figures 1 and 2). Because this storm comprised 4 substorms, we detected the substorm phases by timing each of the 4 substorms. Following [14, 15], we will term these phases the growth phase (1), the actively-convective phase (2), the expansion (explosive) phase (3), and the recovery phase (4).

(a)

(b)

(c)

Figure 1: (a) AE-index for the chain of substorms, May 3, 1986. Timing of the chain of substorms CDAW9C [13]. Single and double asterisks indicate the actively convective phase and the expansion (explosive) phase of the substorm, respectively. (b) Dst-index for the chain of CDAW9C substorms [13]. (c) Estimations of power of Joule heating of the ionosphere and power of particles precipitation into the ionosphere for the chain of CDAW9C substorms.

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(b)

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Figure 2: ((a), (b), and (c)) Timing of the chain of substorms CDAW9C. Magnetograms of the ground-based magnetometers for the chain of substorms; May 3, 1986. Single and double asterisks indicate the actively convective phase and the expansion (explosive) phase of the substorm, respectively [13].

In summary, the data on the 1986 May 3 event (Figures 1 and 2) could be used to trace each substorm phase contribution (energy loading-unloading) to the composite set of processes in the lower atmosphere.

The 1989 March 13-14 magnetospheric storm refers to one of the strongest magnetospheric storms observed since the space era onset and occurred during solar Cycle-22, see, for example, [16, 17]. The geomagnetic storm reached the maximal intensity on 1989 March 13 when the Dst-index reached a record value of about −600 nT [16, 17]. To save space, we do not give the illustrations for the 1989 March 13-14 event here. There are many papers describing this storm.

The 2003 October-November solar activity sharp burst led to strong magnetospheric storms with the 2003 October 28–31 high AE-index values and Dst-index of about −400 nT [18]. For the reasons above, we do not give the illustrations for this event here.

3. Discussion and Conclusions

As one can see (Figures 1, 3, and 4), the ionosphere underwent rather a significant Joule heating with a great power of precipitating energetic particles. Nevertheless, there were no abnormal variations in the lower atmosphere meteoparameters. The variations in physical characteristics of hurricanes (wind velocity, temperature, and pressure distribution) were not associated with high magnetic activity both in the high-latitude regions and in the mid-latitude ones (Figures 5, 6, and 7). We have used a lot of data for the analysis; some examples are illustrated in figures. There is no principal difference in plots for the periods of magnetospheric disturbances in comparison to nonstorm days. The atmospheric process power incomparably exceeds energy flux from the solar wind into the geomagnetosphere and the power of extremely strong magnetospheric disturbances. The energy flux from the magnetosphere into the atmosphere during the strong storm was about , which is by 2-3 orders of magnitude less than the atmospheric process power whose values are in [19]. Investigations into the solar activity effect on atmospheric processes have become especially topical recently [7, 20]. But, if there is a mechanism for the magnetospheric disturbance effect on meteorological processes in the atmosphere, it supposes a more complicated series of many intermediates and is not associated directly with the energy that arrives at the ionosphere during storms.

Figure 3: Estimations of power Joule heating and of power of particles precipitation into the ionosphere for the magnetospheric storm, March 13, 1989.

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(b)

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Figure 4: Estimations of power of Joule heating and power of particles precipitation into the ionosphere: (a) October 28, 2003; (b) October 29, 2003; (c) October 30, 2003; (d) October 31, 2003.

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(b)

Figure 5: The NCEP/NCAR reanalysis example for the event, May 3, 1986: (a) height of an isobaric surface at the level 100 hPa (average per day); (b) the average temperature at the level 100 hPa.

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(b)

Figure 6: The NCEP/NCAR reanalysis example for the event, March 13-14, 1989: (a) height of an isobaric surface at the level 100 hPa (average per day); (b) the average temperature at the level 100 hPa.

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Figure 7: The NCEP/NCAR reanalysis example for the event, October 30, 2003: (a) height of an isobaric surface at the level 100 hPa (average per day); (b) the average temperature at the level 100 hPa.

The main result of our investigation (see Table 1) is that the 1989 March magnetic storm did not directly affect the tropical cyclogenesis evolution character (Figures 8, 9, and 10). As for the 2003 October-November storms, one cannot answer unambiguously, either, because 5 plus intense and long-lived cyclones were observed then. The 13 October–1 November strong storm in the North Atlantic had existed extremely long (19 days), taking into account that the cyclone life average duration in Atlantic is 9 days. In 2003 October, 3 tropical cyclones were observed in the East Pacific: Hurricane Nora (October 1–9, the maximal wind being 41 m/s); Tropical Storm Olaf (October 3–8, 30 m/s); Tropical Storm Patricia (October 20–26, 31 m/s). However, all of the strong storms in the East Pacific were observed prior to the magnetic storm onset.

Table 1

Region
1986
1989
2003

Northern Atlantic
June, August, September, November
June, July, August, September, October, November, December
April, June, July, August, September, October, November, December

Eastern Pacific
May, June, July, August, September, October
January, May, June, July, August, September, October
January, May, June, July, August, September, October

Western Pacific
Throughout the year
January, April, May, June, July, August, September, October, November, December
April, May, June, July, August, September, October, November, December

We indicate the months when storms were observed in those years. As seen from the table, the storm was observed in the Eastern Pacific in May 1986. It had existed May 22–29 which cannot be associated with the May 3, 1986 magnetic storm. Yet, it corroborates the climatology of tropical cyclone (tropical cyclones originate in the Pacific Ocean, May through November).

(a)

(b)

(c)

Figure 8: (a) The example of the trajectory of the cyclone observed in the North Atlantic, for events in 1989. (b) The example of the trajectory of the cyclone observed in Eastern Pacific, for events in 1989. (c) The example of the trajectory of the cyclone observed in Western Pacific, for events in 1989.

Figure 9: The trajectory of the cyclone observed in the North Atlantic 13 October–1 November, 2003. This storm was observed during the magnetic storm and has existed maximum for a long time (19 days) at average life time of a cyclone, which is 9 days, in the North Atlantic.

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(b)

Figure 10: (a) The example of trajectories of the cyclone observed in Eastern Pacific. In October, 2003, in East part of Pacific ocean 3 outputs of a tropical cyclone were observed: Hurricane Nora, October, 1–9, 2003, with the maximal speed of wind –41 m/s; Tropical Storm Olaf, October, 3–8, 2003, with maximal wind speed of 30 m/s; Tropical Storm Patricia, October, 20–26, 2003, with the maximal wind speed of 31 m/s. All storms were observed prior to the beginning of action of the magnetospheric storm. (b) The example of trajectories of the cyclone observed in Western Pacific for events in 2003. In October-November, 2003, more than 5 intensive and long cyclones were observed.

Cloud layers play an important role in Earth’s radiation balance [21–23], affecting the amount of heat from the Sun that reaches the surface and the heat radiated back from the surface that escapes out into space. One should pay special attention to the effect of the solar wind electric field sharp increase (via the global electric circuit during magnetospheric disturbances) on the cloud layer formation. It is necessary to test the assumptions that this layer may function as a screen decelerating radiative cooling of the air located on the Central Antarctic ice dome (as a result, there would be warming in the ground atmospheric layer and cooling above the cloud layer [24]). Authors in the paper [24] suggested that the interplanetary electric field influences the katabatic system of atmospheric circulation (typical of the winter in the Antarctic), via the global electric circuit affecting clouds and hence the radiation dynamics of the troposphere.

Let us briefly address the problem of the extraneous electric field penetration into the Earth’s magnetosphere. More than five decades ago, Dungey [25] suggested the following model for the magnetospheric electric field generation. The solar wind magnetic field partially permeates inside the magnetosphere therefore, the polar cap field lines leave for the solar wind. In the solar wind, there is the electric field , where is the solar wind velocity and is the interplanetary magnetic field. Because the conductance along field lines is very high, the electrical potential associated with the field in the solar wind is transported into the polar cap ionosphere. In the polar cap, a Sun-away convection originates, and, for that convection to be closed, reverse motions on closed field lines of the inner geomagnetosphere are necessary. Two-vortex convection was assumed to be obtained. Through multiplying the solar wind electric field value by the geomagnetosphere size towards dawn-dusk being about 25–30 Re (Re~6371 km) and through assuming the solar wind velocity as ~450 km/s, we will obtain the potential difference between the dawn and the dusk sides of the magnetosphere , (kV) which is manifold less than the well-known experimental formula [26] (nT) provides.

The penetration of the electric field and the current into the geomagnetosphere is a two-stage process and may be presented as follows (see Figure 11). Let an electric current component towards the magnetosphere appear at instant T. A potential value will be established at the magnetopause segment. In the thin near-side layer of the thickness (where is proton plasma frequency and is the speed of light), the charge division process will start, and the displacement current will appear. Also, there will appear Ampere force that will start accelerating plasma. The only force that withstands the Ampere one is the inertia force. Under the conditions of a homogeneous medium, the inertia force is :

Figure 11: The scheme of the penetration of the external electric current and electric field in the magnetospheric plasma and generation of magnetospheric convection. In the figure, the part of magnetopause, through which the electric current and the electric field will penetrate, is shown.

Taking into account that , where is the Alfven velocity, upon integrating we will have that is, the classic equation for the electric drift velocity (it is important for us to express the dynamic process in this case).

When the plasma is accelerated in the layer up to the drift velocity (and it happens during the gyroperiod), then there will be no field in the plasma coordinate system, and it appears at the boundary between the moving and stable plasmas in a stable coordinate system (see Figure 11). The boundary moving velocity separating the moving plasma from the stable one will be, consequently, , where is the proton gyrofrequency. Taking the values and into the equation for the phase velocity, we see that it is the Alfven velocity like we expected. Thus, the external electric field penetrates into the magnetosphere without any limitations of the Alfven-wave type, and the electric current is only in a form of the displacement current. The electric current flows through the system under consideration only when there is a transitive process. In the stationary regime, there is no electric current. If the magnetic field is inhomogeneous according to an axis , then the gas pressure gradient will be originated independently due to the flow nonuniformity. The electric field establishment time in the system here is , and the current establishment time is , where is the system size, is the phase velocity for the electromagnetic signal propagation across the system, , and is the plasma convection velocity. An approximate estimate applied to the magnetosphere gives the time of the electric field establishment to be hundreds of seconds and the electric current establishment time to be about an hour. Thus, the electric current penetration into plasma is a two-stage process. Initially, the polarization field that penetrates into plasma “layer by layer” is produced. Or, to be more exact, the momentum corresponding to this field penetrates into plasma. Here, if the system is inhomogeneous, the flow can redistribute pressure so that an electric current arises in plasma because of the appearance of gradients. This electric current is necessary to maintain plasma convection in the magnetosphere [27, 28].

Indeed, there is no simple global electric circuit via which a sharp increase in the solar wind electric field during magnetospheric disturbances would be possible. The solar wind electric field penetration process is complex and nonlinear. Field-aligned currents connect the magnetosphere and the ionosphere in the united electric circuit. The plasma convection generation in the geomagnetosphere is associated with the processes at the bow shock front [27]. The combined action of plasma convection and pitch-angle diffusion of electrons and protons leads to the formation of plasma pressure distribution in the magnetosphere. As known, steady electric bulk currents are associated with the gas pressure distribution. The divergence of these bulk currents causes a spatial distribution of field-aligned currents, that is, magnetospheric sources of the ionospheric electric current systems [29]. The atmospheric conductivity sharply declines between the polar ionosphere and the layer at h~10 km.

The geomagnetospheric disturbance effect on the troposphere is weak compared with a multitude of other factors affecting it. However, the existing works on a high correlation between tropical cyclones and magnetic storms may evidence either the existence of another mechanism for the effect (that was not addressed in this study) or a random coincidence rather than a physical essence. A very interesting mechanism suggested by Troshichev and Janzhura [24] needs further considering and improving. Authors in the paper [24] noted that the solar wind dynamic pressure effect on the cloud layer would be opposite to that of the interplanetary electric field. Thus, now we can note that, probably, there is some connection between processes at the bow shock front region and meteorological processes at the lower atmosphere, because the magnetospheric plasma convection generation is associated with processes at the bow shock front (e.g., see [27]).

A further study of geomagnetospheric storm effects on tropical cyclogenesis is necessary, because the character of some influence has regional peculiarities (see Figures 8–10). In the next paper, we are going to investigate a probable effect of such magnetospheric disturbances as sawtooth events, extraordinary powerful magnetic storms, and some others on meteorological processes in the lower atmosphere.

Acknowledgments

This study was supported by the Russian Foundation for Basic Research, Project no. 12-05-31096 mol_a. The authors are grateful to creators and developers of the following websites: (1) http://www.nhc.noaa.gov/pastall.shtml; (2) http://www.csc.noaa.gov/hurricane_tracks; (3) http://www.aoml.noaa.gov/hrd/hurdat/ushurrlist18512007.txt; (4) http://russian.wunderground.com/hurricane/hurrarchive.asp?region=at; (5) ftp://ftp.cdc.noaa.gov/; (6) http://www.kosmofizika.ru/; (7) http://www.viems.ru/asnti/ntb/ntb502/oboc5.html for providing observational data.

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