Open Access

Complex inner core boundary from frequency characteristics of the reflection coefficients of PKiKP waves observed by Hi-net

Progress in Earth and Planetary Science20152:34

DOI: 10.1186/s40645-015-0064-3

Received: 21 April 2015

Accepted: 8 October 2015

Published: 4 November 2015


Frequency-dependent reflection coefficients of P waves at the inner core boundary (ICB) are estimated from the spectral ratios of PKiKP and PcP waves observed by the high-sensitivity seismograph network (Hi-net) in Japan. The corresponding PKiKP reflection locations at the ICB are distributed beneath the western Pacific. At frequencies where noise levels are sufficiently low, spectra of reflection coefficients show four distinct sets of characteristics: a flat spectrum, a spectrum with a significant spectral hole at approximately 1 or 3 Hz, a spectrum with a strong peak at approximately 2 or 3 Hz, and a spectrum containing both a sharp peak and a significant hole. The variety in observed spectra suggests complex lateral variations in ICB properties. To explain the measured differences in frequency characteristics of ICB reflection coefficients, we conduct 2D finite difference simulations of seismic wavefields near the ICB. The models tested in our simulations include a liquid layer and a solid layer above the ICB, as well as sinusoidal and spike-shaped ICB topography with varying heights and scale lengths. We find that the existence of a layer above the ICB can be excluded as a possible explanation for the observed spectra. Furthermore, we find that an ICB topographic model with wavelengths and heights of several kilometers is too extreme to explain our measurements. However, restricting the ICB topography to wavelengths and heights of 1.0–1.5 km can explain the observed frequency-related phenomena. The existence of laterally varying topography may be a sign of lateral variations in inner core solidification.


Inner core boundary Topography PKiKP Finite difference modeling


The inner core boundary (ICB) is one of the vital regions for understanding the Earth’s core dynamics (Loper and Roberts 1981; Loper 1983; Bergman and Fearn 1994; Shimizu et al. 2005; Deguen et al. 2007; Sumita and Bergman 2009; Deguen 2012). Seismological studies of the ICB and its inferred characteristics, such as the density jump between the inner and the outer cores, the shear-wave velocity at the top of the inner core, and scattering of seismic energy from small-scale topography at the inner core surface, are important in elucidating the growth mechanism of the inner core and the source of the geodynamo (Souriau 2007; Sumita and Bergman 2009; Deuss 2014; Tkalčić 2015).

The hypothesis of a hemispherical structure in the upper inner core (Tanaka and Hamaguchi 1997) has been widely accepted because it is supported by seismic observations of body waves and free oscillations (Creager 1999; Deuss et al. 2010). Hemispherical dichotomy is recognized as a global phenomenon near the ICB (Niu and Wen 2001; Waszek et al. 2011) and possibly near the center of the inner core (Lythgoe et al. 2014). To explain the hemispherical structure of the inner core, two models have been proposed: a large-scale asymmetric flow in the outer core (Sumita and Olson 1999; Aubert et al. 2008; Gubbins et al. 2011) and translational convection in the inner core (Alboussiere et al. 2010; Monnereau et al. 2010). The nature of these models is that they allow diametrically opposite scenarios of freezing and melting, i.e., one of the two hemispheres solidifies faster than the other. This has raised further questions about whether the surface of the inner core in the eastern hemisphere is melting or freezing. Although translational convection models predict that the eastern hemisphere is melting, outer-core large asymmetric flow models disagree about which hemisphere is melting, due to the problem setting, e.g., heat flux at the core–mantle boundary (CMB) and outer core dynamics.

Measurements of PKiKP/PcP amplitude ratios have been used to infer the density jump at the ICB, as well as to determine the shear velocity at the top of the inner core. A sketch of their ray paths is shown in Fig. 1. Studies in the twentieth century usually analyzed PKiKP recorded on short-period seismographs with a predominant frequency of 1 Hz (Engdahl et al. 1970; Buchbinder 1972; Engdahl et al. 1974; Souriau and Souriau 1989; Shearer and Masters 1990). These pioneering studies may have been hampered by the small number of observations and the large scatter in PKiKP/PcP amplitude ratios due to the nature of noisy amplitude measurements (Tkalčić et al. 2009). Another factor influencing the amplitude ratios, and possibly the anti-correlation between the two phases, is the occurrence of near-receiver crustal and mantle heterogeneity (Tkalčić et al. 2010).
Fig. 1

Ray paths of PcP and PKiKP seismic phases. A cross section of Earth with ray paths of PcP and PKiKP seismic phases originating at the source (star) and recorded by a station at the Earth’s surface

The new era of modern instruments, dense networks, and improved global coverage enables observation of a large number of PKiKP and PcP phases on the same seismogram. For example, Koper et al. (2003) analyzed a significant number of PKiKP phases at shorter distances recorded by small aperture arrays of the International Monitoring System. This study was followed by a large number of new studies (Cao and Romanowicz 2004; Koper et al. 2004; Koper and Pyle 2004; Poupinet and Kennett 2004; Koper and Dombrovskaya 2005; Krasnoshchekov et al. 2005; Leyton et al. 2005; Kawakatsu 2006; Leyton and Koper 2007a, b; Peng et al. 2008).

More specifically, Koper and Pyle (2004) measured PKiKP/PcP amplitude ratios from seismograms filtered between 1 and 3 Hz. Their analysis did not reveal any differences between the eastern and western hemispheres of the inner core. Using phases from a Mariana event observed in Japan, whose raypaths sampled the ICB beneath the western Pacific, Kawakatsu (2006) found little scattering energy in the PKiKP coda. However, Leyton and Koper (2007b) analyzed the coda of PKiKP and suggested the existence of small-scale heterogeneities in the uppermost inner core. This result indicates that the strong scattering region is located beneath the Pacific Ocean and Asia, which covers parts of the eastern and western hemispheres. On the basis of scattering properties and Q structure, Cormier (2007) inferred textural differences between the eastern and western hemispheres near the surface of the inner core, including vertically oriented structures in the eastern hemisphere.

Interestingly, the existence of a high-frequency PKiKP phase (up to 5 Hz) with steep incidence angles at the ICB was first observed by Poupinet and Kennett (2004) using phases recorded by narrow-aperture arrays and temporal broadband networks on the Australian continent, whose reflection points were in the eastern hemisphere. Recently, the same class of PKiKP waves was observed in the eastern hemisphere on Chinese and Japanese short-period and broadband stations (J-array) (Tkalčić et al., 2009, 2010) and by the high-sensitivity seismograph network (Hi-net) in Japan (Dai et al. 2012, Jiang and Zhao 2012).

To contribute to a better understanding of inner core dynamics and to constrain ICB structure in the eastern hemisphere, here, we collect an extensive dataset of PKiKP waves recorded by Hi-net in Japan. Our aim is to shift focus from analyzing a single value of the PKiKP/PcP amplitude ratio to evaluating its broad frequency characteristics, which is philosophically similar to how Cummins and Johnson (1988) evaluated pre-critical PKiKP waveforms and spectra by using a hybrid full wave-reflectivity algorithm. A dense configuration of borehole seismograms with high SNR observations of PKiKP waves over an unusually broad range of frequencies facilitates this new approach to estimate ICB properties. Thus, we examine data in the frequency domain and investigate possible broader implications for Earth’s core dynamics.


Hi-net comprises approximately 700 short-period seismographs placed at the bottoms of individual boreholes (Okada et al. 2004). However, even for large-volume datasets such as Hi-net, good records of PKiKP and PcP are not frequently observed. We have detected PcP and PKiKP waveforms from 11 earthquakes with body wave magnitude ≥5.8 and focal depths of ≥80 km around Japan before the 2011 Tohoku earthquake (Fig. 2, Table 1). This covers epicentral distances from 15° to 50°. The reflection points of PKiKP at the ICB are distributed beneath the western Pacific, which is part of the eastern hemisphere (Fig. 2).
Fig. 2

Study area. Map view of epicenters (stars) and PKiKP bounce points at the ICB (green circles). Event numbers are taken from Table 1

Table 1

Event list



Time (UTC)

Lat. (°)

Lon. (°)

Depth (km)



No. of used records




































































































Hypocenters are taken from the Earthquake data report provided by U.S.G.S.

DC double couple, Sm smoothed radiation pattern

After visual examination of waveforms, amplitude spectra of PKIKP phases, and corresponding waveforms and spectra of pre-arrival noise, we applied a zero-phase Butterworth band-pass filter with corner frequencies of 2 and 5 Hz to 60 s record segments centered around theoretical PKiKP arrival times (Fig. 3a, b). This was done for all records except the Mariana event (event 1), which was examined by Kawakatsu (2006) and observed to have large PKiKP signals around 1 Hz. Note that we use band-pass filtering only for initial identification of PKiKP.
Fig. 3

Selection of coherent waveforms. a Raw seismograms of event 3 recorded by Hi-net stations whose names start with letter “I.” Horizontal axis is the lapse time from the theoretical arrival times of PKiKP. b Seismograms from a are band-pass filtered with cutoff frequencies of 2 and 5 Hz. c The selected set of coherent waveforms after employing the cross-correlation matrix method (Tkalčić et al., 2011) is shown by cyan lines

After applying the band-pass filter described above and retrieving record segments of ±10 s length around PKiKP arrivals, seismograms were divided into sub-groups comprising 70–230 stations with traces sorted by increasing epicentral distance. We then selected subsets of coherent waveforms by using the cross-correlation matrix method (Tkalčić et al. 2011), which retained 46–220 records per event. To find coherent PKiKP arrivals in each sub-group, we empirically determined the minimum percentage (τ) of all waveform pairs that should cross-correlate in such a way that the average cross-correlation coefficient equals or exceeds a threshold β. The algorithm calculates the cross-correlation coefficients for each pair of waveforms and counts the total percentage of pairs with cross-correlation coefficient exceeding β. For example, for β > 0.4, τ > 10 %, and 130 total waveforms, we found that 77 waveforms satisfied these criteria and were consequently selected as “mutually coherent” (Fig. 3c). Incoherent waveforms were not used in further analyses. Subsequently, we visually checked the waveforms that satisfied the above criteria to find possible PKiKP signals with high signal-to-noise ratios, which resulted in a station list of “good” sites for PKiKP observations.

In the next step, we prepared a spectrogram of 90 s length from the unfiltered seismograms, with a sampling interval of 1 s and a lapse time of 50 s from the theoretical arrival times of PcP or PKiKP (Fig. 4). Each Fourier spectrum is calculated for a Welch tapered 10 s window (Press et al. 1988), then smoothed using a three-point moving average. Using the station list obtained with the cross-correlation matrix method, we used both the seismograms and spectrograms of PKiKP and PcP to identify acceptable data for calculating spectral ratios of PKiKP/PcP (Fig. 5). For each event, between 33 and 83 station records were retained (Table 1). Finally, the mean PKiKP/PcP spectral ratio was computed at each frequency that exceeded the mean of the noise/PcP ratio (Fig. 5). The spectra of PcP and PKiKP contained several peaks and holes whose central frequencies were not uniform for all events. For example, for event 3, the spectral ratio of PKiKP/PcP exceeded the mean noise/PcP ratio in the range 0.8 to 3.0 Hz (Fig. 5a). In the case of other events, however, valid frequency ranges were somewhat different, e.g., 2–3 Hz for event 6 (Fig. 5b) and 1–4 Hz for event 11 (Fig. 5c). Despite the above restrictions, the relatively high-frequency content of the PcP and PKiKP waves means that these high-quality simultaneous observations over a broad frequency interval are unprecedented.
Fig. 4

Spectrograms including PcP and PKiKP. Raw seismograms and spectrograms of event 3 for a PcP and b PKiKP recorded at station IKTH. Spectrogram scaling is in decibels (dB). The predicted arrival times of PcP and PKiKP are located at a lapse time of 50 s

Fig. 5

Spectra of PcP and PKiKP and spectral ratios of PKiKP/PcP. Individual PKiKP, PcP, noise spectra, and PKiKP/PcP spectral ratios for a event 3, b event 6, and c event 11 (see Fig. 2 for the event location). (Top row) Spectra of PcP (blue lines) and PKiKP (red lines), noise in the 20 s window prior to PcP (gray lines), and noise in the 20 s window prior to PKiKP (black lines). Open circles are average spectral amplitudes for PcP, PKiKP, noise prior to PcP, and noise prior to PKiKP at each frequency. (Bottom row) Spectral ratios of PKiKP/PcP (red lines) and noise before PKiKP/PcP (black lines). Open circles are average values of spectral ratios at each frequency

To correct the amplitude ratios, we determined focal mechanisms using the program of Kikuchi and Kanamori (2003), rather than cataloged Global CMT solutions, USGS Moment tensor, and double-couple solutions. The broadband displacements of P and SH waves in the frequency range 0.002–1 Hz were used for the inversion. Furthermore, we compared the short-period (SP) P wave amplitudes (1–5 Hz) with the radiation pattern predicted from each focal mechanism solution. Although the observed SP amplitudes showed a high degree of scatter, we found that some events had clear energy even near the nodal plane and null axis, suggesting a smoothed radiation pattern. This may be due to scattering near the source region, as discussed in previous studies that determined magnitudes from SP data (e.g., (Schweitzer and Kværna 1999; Takemura et al. 2015). These results are summarized in the Remarks column of Table 1. The smoothed radiation pattern for the short period is a likely explanation for the observation of PcP and PKiKP in the events from Kuril (event 2) and Mindanao (event 11), in which the take-off azimuths and angles of PcP and PKiKP were located near the nodal plane.

Attenuation factors for the mantle and core at arbitrary frequencies were normalized to a reference frequency of 1 Hz. We then obtained the corrected relationship between spectral and theoretical amplitude ratios from the following relationship:
$$ {\left(\frac{A_{\mathrm{PK}\mathrm{iKP}}}{A_{\mathrm{PcP}}}\right)}_{\mathrm{corrected}}={\left(\frac{A_{\mathrm{PK}\mathrm{iKP}}}{A_{\mathrm{PcP}}}\right)}_{\mathrm{observed}}\frac{F_{\mathrm{PcP}}}{F_{\mathrm{PK}\mathrm{iKP}}}\frac{ \exp \left(-\pi {f}_0\varDelta {t}^{\ast}\right)}{ \exp \left(-\pi f\varDelta {t}^{\ast}\right)}=\frac{T_{\mathrm{PK}}{R}_{\mathrm{KK}}{T}_{\mathrm{KP}}}{R_{\mathrm{PP}}}\frac{G_{\mathrm{PK}\mathrm{iKP}}}{G_{\mathrm{PcP}}}\frac{ \exp \left(-\pi {f}_0{t^{\ast}}_{\mathrm{PK}\mathrm{iKP}}\right)}{ \exp \left(-\pi {f}_0{t^{\ast}}_{\mathrm{PcP}}\right)}, $$
where the subscripts PKiKP and PcP denote the corresponding seismic phases. On the left side of the equation, A is the spectral amplitude at an arbitrary frequency, F is the focal mechanism radiation pattern, t * is the anelastic parameter (Lay and Wallace 1995), and Δt* is the differential anelastic parameter between PKiKP and PcP. On the right side, G represents the geometrical spreading factor; f 0 (=1 Hz) and f are reference and observed frequencies, respectively; T PK and T KP are the transmission coefficients at the CMB; and R PP and R KK denote reflection coefficients at the CMB and ICB, respectively. The reflection coefficient R KK at the ICB is estimated from the corrected spectral ratios by considering the terms of the reflection and transmission coefficients at the CMB, the geometrical spreading factor, and anelastic parameters, which are calculated using ak135 (Kennett et al. 1995):
$$ {\left({R}_{\mathrm{KK}}\right)}_{\mathrm{estimated}}=\left[{\left(\frac{A_{\mathrm{PK}\mathrm{iKP}}}{A_{\mathrm{PcP}}}\right)}_{\mathrm{corrected}}\right]/\left[\frac{T_{\mathrm{PK}}{T}_{\mathrm{KP}}}{R_{\mathrm{PP}}}\frac{G_{\mathrm{PK}\mathrm{iKP}}}{G_{\mathrm{PcP}}}\frac{ \exp \left(-\pi {f}_0{t^{\ast}}_{\mathrm{PK}\mathrm{iKP}}\right)}{ \exp \left(-\pi {f}_0{t^{\ast}}_{\mathrm{PcP}}\right)}\right]. $$

We converted the spectral ratios to reflection coefficients as a function of frequency. To the first order, geometric spreading is constant with respect to frequency under a ray-theoretical assumption. The reflection and transmission coefficients were then calculated for planar boundaries. The correction of the attenuation factor using t * gives a smooth exponential variation with frequency. Thus, these corrections will not result in any spectral holes or peaks.

To reduce the unwanted effect of the CMB on the PcP spectra, the spectral ratios of PcP/P were examined. Similar to the above procedure, we estimated the P wave reflection coefficients at the CMB as a function of frequency. The obtained reflection coefficients did not always coincide with theoretical values due to the uncertainty in focal mechanisms, large differences in P and PcP take-off angles, and other unknown causes. Thus, we corrected only the fluctuations in the reflection coefficients around the average values in the frequency range 1–3 Hz. The reflection coefficients at the ICB are multiplied by the fluctuations in reflection coefficients at the CMB, which can result in either amplifying an apparently small PKiKP/PcP due to a large peak in the PcP spectrum or reducing a large PKiKP/PcP due to a small peak in the PcP.


A summary of frequency-dependent ICB P wave reflection coefficients, as derived from Eqs. (1) and (2), is shown in Fig. 6. Panels are sorted by increasing incidence angle at the ICB; we refer to each panel hereafter as result n, where n stands exclusively for panel number. Figure 7 summarizes frequency-dependent P wave reflection coefficients at the CMB derived from PcP/P spectral ratios. In Fig. 8, these are used to correct the reflection coefficients at the ICB (Fig. 6). These corrected values are used in finite difference modeling and subsequent interpretation.
Fig. 6

P wave reflection coefficients at the ICB. P wave reflection coefficients at the ICB as a function of frequency, estimated from PKiKP/PcP spectral ratios (red circles) and noise/PcP (black circles). Thin lines show the upper and lower bounds of standard errors. Thick lines are theoretical values of reflection coefficients calculated using ak135 (Kennett et al., 1995). Encircled numbers are “result numbers,” arranged by ascending incidence angle

Fig. 7

P wave reflection coefficients at the CMB. P wave reflection coefficients at the CMB as a function of frequency, estimated from PcP/P spectral ratios (red circles) and noise/P (black circles). Thin lines show the upper and lower bounds of standard errors. Thick lines are theoretical values of the reflection coefficient calculated using ak135 (Kennett et al., 1995). Encircled numbers have the same meaning as in Fig. 6

Fig. 8

Corrected P wave reflection coefficients at the ICB. P wave reflection coefficients at the ICB as a function of frequency, estimated from PKiKP/PcP spectral ratios (red circles) and noise/PcP (black circles). Ratios are corrected for fluctuations estimated from the P wave reflection coefficients at the CMB, obtained from the PcP/P ratios in Fig. 7. Thin lines are upper and lower bounds by standard errors. Thick lines are theoretical values of the reflection coefficient calculated using ak135 (Kennett et al., 1995). Horizontal arrows indicate the effective frequency ranges. Encircled numbers are explained in Fig. 6

The frequency characteristics of the ICB reflection coefficients are quite complex, even in a narrow effective signal band (Fig. 8). Roughly speaking, peaks in reflection coefficients appear around 2 Hz (results 8, 9, and 10) and 3 Hz (result 3), and holes are observed around 1 Hz (results 2, 3, and 4) and 3 Hz (result 10). Although the discrimination is still qualitative, we recognize four general categories of frequency-dependent characteristics: (i) a flat variation, where fluctuations in the relative strengths of peaks and holes are between half and double those of the theoretical reflection coefficients (results 1, 5, 6, 7, and 11); (ii) a distinct single hole in each reflection coefficient spectrum (results 2 and 4); (iii) a strong single peak in each spectrum (results 8 and 9); and (iv) a strong peak and hole in the same spectrum (results 3 and 10).

The geographical distribution of these categories is plotted in Fig. 9. The diameters of the 1 and 2 Hz Fresnel zones for PKiKP are approximately 80 and 60 km at the ICB, respectively. This is equivalent to the area of PKiKP reflection points at the ICB that is covered by a single event and all stations that detect PKiKP. This result suggests that our averaging within each region number is meaningful, but it is not appropriate in discussing lateral variations in individual measurements within each region. Although the sampling areas are sparse, we note a tendency of frequency peaks in reflection coefficient spectra to be most observable at low latitudes (results 8, 9, and 10). Frequency holes show no such latitudinal trend (results 2, 3, 4, and 10).
Fig. 9

Summary map of frequency characteristics of P wave reflection coefficients at the ICB. Distribution of the reflection points of PKiKP waves at ICB (green dots), and “result numbers” indicating their frequency characteristics by colors. White: almost flat spectrum; blue: spectrum with a spectral hole; red: spectrum with a spectral peak; half red and blue: both a hole and a peak. Yellow dots indicate the exit and entrance points of PKiKP at the CMB. Double black and red circles are Fresnel zones at the ICB and CMB, respectively. Inner and outer circles are Fresnel zone estimates for 2 and 1 Hz, respectively


Effects of the CMB

Regarding the effects of the CMB on PKiKP spectra during transmission through the CMB, we address this issue in the context of the results of previous studies. Using amplitude of precursors to PKIKP, Dai et al. (2012) and Yao and Wen (2014) showed that several regions exhibit weak scattering in the lowermost mantle beneath the southwestern Pacific. PKiKP phases from events that occurred in the Banda Sea (events 4 and 9), Sumatra (events 3 and 10), and the Philippines (event 11) enter a “normal” CMB. According to Hedlin and Shearer (2000), there is a relatively weak scattering region in the lowermost mantle beneath the Philippine Sea, which corresponds to the CMB entry points of PKiKP for events 1 and 5 and the CMB exit points for events 1, 3, 4, 5, 9, 10, and 11. Thus, we have reason to believe that the CMB effects on the estimated reflection coefficients for results 1, 2, 6, 8, 9, 10, and 11 will be negligible. However, a strong scattering area near the CMB exists beneath north Japan and the northwestern Pacific, which includes the PKiKP CMB entry and exit points for events 2, 6, 7, and 8. Thus, we cannot rule out the possibility that the frequency characteristics of calculated reflection coefficients for results 3, 4, 5, and 7 are CMB effects, e.g., the high-frequency components of PKiKP may be lost by scattering at the CMB.

Numerical simulations

Problem setup

To explain our observations, we use the 2D finite difference program e3d (Larsen and Shultz 1995; Rodgers et al. 2006) to simulate wave propagation by solving the full wave equation on a staggered grid. The solutions are fourth order accurate in space and second order accurate in time. Figure 10a shows the configuration of the simulation, for which the grid spacing is 70 m. P- and S-wave velocities and densities above and below the ICB are taken from ak135 (Kennett et al. 1995). We place a sequence of point sources with 1 km spacing on a straight line 100 km long and generate a plane wave. The incidence angle θ is a control parameter. As the input, the representative P wave waveform is taken from the Mariana event (event 1). The calculation is valid for frequencies up to 5 Hz. We examine the observed spectral ratios between incident and reflected waves at three points (triangles in Fig. 10a). To verify the configuration and boundary conditions, and to ensure that there are no unwanted numerical effects from the edges of the box, we conducted a test run of a simple, flat ICB, with elastic parameters on both sides of the ICB taken from the ak135 model (Fig. 10b). The spectral ratios between upgoing and downgoing waves for incidence angles of 10°, 20°, and 30° correspond to epicentral distances of approximately 16°, 32°, and 48°, respectively. Although there are small frequency-dependent fluctuations (within a factor of 2, at most), their average values coincide well with the theoretical reflection coefficients at the ICB.
Fig. 10

Configuration of 2D finite difference simulations and a test run. a Configuration of 2D finite difference simulations using e3d (Larsen and Shultz 1995). Small red circles represent multiple sources used to simulate a plane wave. Triangles mark the locations of virtual receivers used to record the reflected waves. Incidence angles θ are a control parameter. b Spectral ratios between upward and downward waves using a flat discontinuity in simulations for incidence angles of 10°, 20°, and 30°. Thick lines are theoretical values of the reflection coefficient calculated using ak135 (Kennett et al. 1995)

Simulations for a thin layer above the ICB

As discussed in the “Background” section, there are multiple conceptual models that can explain freezing and melting of the quasi-eastern hemisphere. To investigate the possibility of a thin layer above the ICB, we run a series of simulations with layer thicknesses of 0.1, 0.25, 0.5, 0.75, 1.0, 3.0, and 5.0 km. For a solid layer above the ICB with finite shear-wave velocity and slight variations in compressional wave velocity and density (Vp = 10.6–10.9 km/s, Vs = 1–3 km/s, ρ = 12.4–12.5 g/cm3), all the resultant reflected wave amplitudes are small. However, a light or heavy liquid layer (Vp = 9.6–10.3 km/s, ρ = 12.5 g/cm3 for heavy liquid, ρ = 11.5 g/cm3 for light liquid) results in large amplitudes. In particular, we find that the amplitudes of seismograms filtered with central frequencies of 1 and 2 Hz become large when we insert a heavy liquid layer above the ICB with Vp = 9.6 km/s, ρ = 12.5 g/cm3, and a thicknesses of 0.75 or 1 km (Fig. 11a, b). This finding is qualitatively consistent with the results of Krasnoshchekov et al. (2005). However, we also find that spectral ratios continuously increase as a function of frequency for any incidence angle (Fig. 11c), without distinct peaks or holes in the frequency range 0.5 to 3 Hz. Since this does not explain our observations, we reject the model of a thin layer above the ICB as a possible explanation for the observed frequency-domain characteristics of PKiKP.
Fig. 11

Results of numerical simulations for a liquid thin layer above the ICB. Maximum amplitudes of the reflected waves measured on seismograms filtered around 1 and 2 Hz as a function of increasing angular distance at the ICB. Synthetic seismograms are calculated by including a heavy liquid layer (Vp = 9.6 km/s, ρ = 12.5 g/cm3) overlying the ICB with varying thicknesses: a 0, 1000, 3000, and 5000 m and b 100, 250, 500, and 750 m. c Spectral ratios for the 1000 m-thick heavy liquid layer for incidence angles of 10°, 20°, and 30°

Simulations for topography at the ICB

Earlier PKiKP and PcP amplitude ratio analyses made sporadic seismological observations of a lower density contrast at the ICB than predicted values for spherically symmetric Earth models, as low as 200–300 g/m3(Koper and Pyle 2004; Tkalčić et al. 2009). In addition, Gubbins et al. (2008) inferred a low density contrast from geodynamical considerations. These results indirectly support the existence of a dense layer at the top of the inner core (F-layer) to explain the smaller density differences between the outer and inner cores. However, there is no proof from seismology that such a layer is a global feature. Masters and Gubbins (2003) noted that even the relatively large density jump inferred from free oscillation analyses is consistent with an F-layer having a strong density gradient: the free oscillation data would average over thick layers below and above the ICB, while the body wave would be sensitive to variations across the ICB. A lower density contrast across the ICB would permit larger topography (Buffett 1997). Of particular interest is the possibility of sharp edges between the solidification and melting areas. Recent waveform modeling suggests significant topography (Dai et al. 2012); however, determination of the amplitude is a more difficult problem than determination of the wavelength.

One possibility of most simplified geometry is that a sinusoidal topographic structure might develop at the largest scales (λ = 10–100 km) (Buffett 1997). At these length scales, there is an inverse relationship between relaxation time scale and wavelength (Turcotte and Schubert 2002). In addition, the time scale required for topography to relax varies inversely with density contrast and linearly with viscosity. As the viscosity of the outer core is effectively zero (de Wijs et al. 1998), the rate of relaxation is thus entirely controlled by deformation in the inner core.

On the other hand, spike-shaped topographic structures might develop as a result of dendritic growth, likely at smaller scales (λ = 10–several 100 m) (Bruce Buffett, pers. comm.). Such topography could be relaxed through melting and freezing (thermal relaxation). As the temperature gradients are steeper at short wavelengths, this can drive the heat flow needed to melt or freeze.

Given the above, we test two different classes of topography at the ICB. In the first scenario, we test a regular sinusoidal topography with wavelength λ and height H (Fig. 12a). The values of (λ, H) tested, in kilometers, are (0.1, 0.1), (0.2, 0.2), (0.5, 0.5), (1.0, 1.0), (1.5, 1.5), (2.5, 2.5), (2.5, 2.6), (2.5, 2.7), (5.0, 2.5), and (10.0, 5.0). Figure 13 shows the results of selected combinations of λ and H. The topographies with λ = 0.1 and 0.2 km and H = 0.1 and 0.2 km did not reproduce any spectral peaks and holes and yielded spectra similar to those obtained from a simple discontinuity model (Fig. 10b). However, for a slightly more prominent topography of λ = 0.5 km and H = 0.5 km, we find a clear peak in spectral ratios around 1.2 Hz (Fig. 13a). The ICB topography with λ = 1.0 and H = 1.0 km results in an increased number of spectral peaks (Fig. 13b). The topographic model with λ = 1.5 and H = 1.5 km produces distinct peaks around 2 Hz for incidence angles of 20° and 30° and remarkable holes around 1.2 Hz for incidence angles of 10° and 30° (Fig. 13c). The best results are obtained for the topography characterized by λ = 1.5 and H = 1.5 km. The simulated spectra contain similar characteristics to those observed in the reflection coefficient profiles of results 8, 9, and 10. However, when the longer λ and larger H are used in simulations (e.g., λ = 5 and H = 2.5 km; λ = 10 and H = 5 km), the reflection coefficients overall become smaller than those for the flat ICB. The spectra are devoid of peaks at higher frequencies (Fig. 13d, e).
Fig. 12

Diagram of ICB topography. Diagram of ICB topography used in numerical simulations with wavelength and height defined as λ and H, respectively. a Sinusoidal topography; b “spiky” topography. The meaning of each topographic model is explained in the text

Fig. 13

Results for sinusoidal topographies. Representative results, characterized by height H and length λ, for incidence angle 10 degrees (left), 20 degrees (middle) and 30 degrees (right). The values of H and lambda are as follows: a) λ = 0.5, H = 0.5, b) λ = 1.0, H = 1.0, c) λ = 1.5, H = 1.5, d) λ = 5, H = 2.5, e) λ = 10 H = 5

Finally, we introduce “spiky” topography to address the possibility of dendritic growth of the inner core (Sumita and Bergman 2009), which is mathematically expressed in our simulations by a reversed cycloid with upward sharp tips (Fig. 12b). We tested several (λ, H) combinations for this conceptual model: (0.1, 0.1), (0.2, 0.2), (0.5, 0.2), (0.5, 0.1), (0.5, 0.2), (1.0, 0.2), (1.0, 0.5), (1.0, 1.0), (1.0, 2.0), (1.2, 1.7), (1.5, 1.5), (1.5, 2.0), (2.0, 1.0), (2.0, 1.5), (2.0, 2.0), and (5.0, 2.0). The overall characteristics of the spectral ratios for spiky topography, with λ ≤ 2 km and H ≤ 2 km (Fig. 14a–d), can be summarized as a gradual decrease in spectral ratio as frequency increases from 0.5 to 5 Hz. This topographic model can explain several peaks or holes for incidence angles of θ = 10° and 20° and many peaks at frequencies around 2, 3, and 4 Hz for θ = 30°. The topography with λ = 5 km and H = 2 km results in relatively flat and small spectral ratios in the frequency range 0.7–5 Hz. Such a model can explain many holes at frequencies larger than 2.5 Hz for θ = 10°–20° and peaks for θ = 30°. However, these results cannot adequately explain our observations because the overall reflection coefficients are too small.
Fig. 14

Results for spiky topographies. Same as Fig. 13, but “spiky” topography was used in simulations. The values of H and λ are as follows: a) λ = 0.5, H = 0.5, b) λ = 1, H=1, c) λ = 1.5, H = 1.5, d) λ = 2, H = 2, e) λ = 5 H = 2

The resultant characteristics are slightly different from those produced by the sinusoidal topographies, even though their structural dimensions are the same. The frequencies of the distinct spectral peaks decrease with increasing wavelength and height (Fig. 14b–d), whereas no distinct peaks are observed for the topography with λ = H = 0.5 km. The spiky topography with λ = H = 1.0 km results in a distinct peak around 1.7 Hz for θ = 10°–20° and a large hole around 1.5 Hz for θ = 30° (Fig. 14b). The topography with λ = 1.5 and H = 1.5 km yields a distinct single peak at roughly f = 1.2 Hz. There are several spectral holes for θ = 10°–20° and peaks for θ = 30° at f > 2 Hz (Fig. 14c). Of all the test cases with spiky topography, the case with λ = H = 1.0 km most closely matches the observed spectral ratios.

In summary, our observations and numerical simulations suggest that the inner core boundary is a sharp boundary without transitional layers. The hypothesis of melt at the surface of the inner core in the quasi-eastern hemisphere is not supported by our simulations. The most likely scenario to explain some of the observed spectral characteristics is the existence of topography at the ICB; however, more than one class of topography must be invoked to explain all observations. We therefore conclude that the topography characteristics of the ICB vary laterally. These variations may result from lateral variations of inner core solidification. If solidification is dynamically driven from top to bottom, its geographical pattern will be controlled by the pattern of outer core convection (Bergman et al. 2002; Aubert et al. 2008; Gubbins et al. 2011). If the solidification is instead driven from the bottom up, the pattern will be affected by variations in inner core convection (Deguen and Cardin 2011). Furthermore, small-scale variations in topographic characteristics suggest small-scale convection in a mushy zone at the ICB (Bergman and Fearn 1994; Deguen et al. 2007). While we cannot distinguish between these hypotheses in the present study, largely due to the fact that we sample only sparse and limited areas of the ICB, further observations of PKiKP and PcP will improve our understanding of large-scale ICB structure and dynamics.


Frequency characteristics of ICB reflection coefficients were investigated for the area around Japan using Hi-net vertical component seismograms. We found four patterns in the frequency-dependent behavior of reflection coefficients: (a) a nearly flat spectrum (little variation), (b) a significant hole at a frequency of approximately 1 or 3 Hz, (c) a peak at a frequency of approximately 2 or 3 Hz, and (d) the existence of a hole and a peak. The variety in observed spectra reflects the complex nature of the ICB. To interpret these observations, we conducted 2D finite difference simulations. Since we tested only limited cases with planar geometry, further simulations are required. Our modeling results suggest that holes and peaks in the spectra of reflection coefficients can be qualitatively explained by a sinusoidal or spike-like topography at the ICB, with wavelengths and heights ~1–1.5 km, whereas a liquid or solid layer overlying the ICB does not reproduce any of the observed spectral features.



core–mantle boundary


inner core boundary



The authors are grateful to the National Research Institute for Earth Science and Disaster Prevention (NIED), Japan, for providing high-quality seismograms recorded by the high-sensitivity seismograph network (Hi-net). The authors thank two anonymous reviewers who give valuable comments. S.T. was supported in part by MEXT KAKENHI grant number 15H05832. H.T. was supported by the Japan Society for the Promotion of Science and the Research School of Earth Science, The Australian National University during his stay in Japan. Most of the figures were drawn using GMT (Wessel and Smith 1998).

Open AccessThis article is distributed under the terms of the Creative Commons Attribution 4.0 International License (, which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.

Authors’ Affiliations

Department of Deep Earth Structure and Dynamics Research, Japan Agency for Marine-Earth Science and Technology
Research School of Earth Sciences, The Australian National University


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