**Research article**| 21 Oct 2022

# Comparison of straight-ray and curved-ray surface wave tomography approaches in near-surface studies

Mohammadkarim Karimpour Evert Slob and Laura Valentina Socco

^{1},

^{2},

^{1}

**Mohammadkarim Karimpour et al.**Mohammadkarim Karimpour Evert Slob and Laura Valentina Socco

^{1},

^{2},

^{1}

^{1}Department of Environment, Land and Infrastructure Engineering, Politecnico di Torino, Turin, 10129, Italy^{2}Department of Geoscience and Engineering, Delft University of Technology, Delft, 2628 CN, Netherlands

^{1}Department of Environment, Land and Infrastructure Engineering, Politecnico di Torino, Turin, 10129, Italy^{2}Department of Geoscience and Engineering, Delft University of Technology, Delft, 2628 CN, Netherlands

**Correspondence**: Mohammadkarim Karimpour (mohammadkarim.karimpour@polito.it)

**Correspondence**: Mohammadkarim Karimpour (mohammadkarim.karimpour@polito.it)

Received: 29 Apr 2022 – Discussion started: 13 May 2022 – Revised: 31 Aug 2022 – Accepted: 08 Sep 2022 – Published: 21 Oct 2022

Surface waves are widely used to model shear-wave velocity of the subsurface. Surface wave tomography (SWT) has recently gained popularity for near-surface studies. Some researchers have used straight-ray SWT in which it is assumed that surface waves propagate along the straight line between receiver pairs. Alternatively, curved-ray SWT can be employed by computing the paths between the receiver pairs using a ray-tracing algorithm. The SWT is a well-established method in seismology and has been employed in numerous seismological studies. However, it is important to make a comparison between these two SWT approaches for near-surface applications since the amount of information and the level of complexity in near-surface applications are different from seismological studies. We apply straight-ray and curved-ray SWT to four near-surface examples and compare the results in terms of the quality of the final model and the computational cost. In three examples we optimise the shot positions to obtain an acquisition layout which can produce high coverage of dispersion curves. In the other example, the data have been acquired using a typical seismic exploration 3D acquisition scheme. We show that if the source positions are optimised, the straight-ray can produce S-wave velocity models similar to the curved-ray SWT but with lower computational cost than the curved-ray approach. Otherwise, the improvement of inversion results from curved-ray SWT can be significant.

Surface waves are commonly analysed to build shear-wave velocity (VS) models. Surface wave tomography (SWT) is a well-established method in seismological studies, where numerous researchers have used it to construct subsurface velocity models at global and regional scales by inverting earthquake signals (Woodhouse and Dziewonski, 1984; Ekstrom et al., 1997; Ritzwoller and Levshin, 1998; Boschi and Dziewonski, 1999; Simons et al., 1999; Boschi and Ekstrom, 2002; Yao et al., 2010). Some authors have applied SWT using ambient noise cross-correlation to retrieve regional crustal structures (Shapiro et al., 2004; Lin et al., 2008; Kästle et al., 2018).

The SWT usually consists of three steps (Yoshizawa and Kennett, 2004; Yao et

al., 2008). First, different path-averaged dispersion curves (DCs) are computed for different receiver pairs aligned with a source. Then, the DCs are inverted to build phase velocity maps at different periods (frequency). Finally, the obtained phase velocity maps are inverted to produce 1D VS models at different locations. However, the efficiency of SWT can be increased by the direct inversion of the path-averaged DCs, i.e. skipping the intermediate step of building phase velocity maps (Boschi and Ekstrom, 2002; Boiero, 2009; Fang et al., 2015).

Traditionally, in seismology SWT has been employed assuming great-circle propagation of surface waves (Trampert and Woodhouse, 1995; Ekstrom et al., 1997; Passier et al., 1997; Ritzwoller and Levshin, 1998; Boschi and Dziewonski, 1999; van Heijst and Woodhouse, 1999; Simons et al., 1999; Boschi and Ekstrom, 2002; Lin et al., 2008; Yao et al., 2010; Bussat and Kugler, 2011; Kästle et al., 2018). However, some researchers have employed SWT not assuming the great-circle propagation of surface waves (Spetzler et al., 2002; Yoshizawa and Kennet, 2004; Lin et al., 2009). SWT has been used in seismological studies for decades and different SWT approaches have been compared by seismologists. For instance, Laske (1995) studied deviations from a straight line in the propagation of long-period surface waves and concluded that they usually have small effects on the propagation phase. Spetzler et al. (2001) applied both straight-ray and curved-ray SWT methods. They computed the maximum deviations of ray paths from straight lines and pointed out that this maximum is typically below the estimated resolution, except for long paths at short periods. Some studies showed that a more complex forward modelling in SWT did not improve the results (Sieminski et al., 2004; Levshin et al., 2005), while other studies reported obtaining better results (Ritzwoller et al., 2002; Yoshizawa and Kennett, 2004; Zhou et al., 2005). Trampert and Spetzler (2006) pointed out that the choice of regularisation has a major impact on SWT results. They studied SWT methods based on ray theory (straight ray and curved ray) and scattering theory in which the integral along the ray path is replaced by the integral over an influence zone. They showed that these methods are statistically alike and any model from one method can be obtained by the other one by changing the value of the regularisation. They concluded that the only option to increase the resolution of the model is to increase and homogenise the data coverage. Bozdag and Trampert (2008) compared straight-ray and curved-ray SWT methods in their study and mentioned that performing ray tracing could be so time-consuming that the potential gain in crustal corrections on a global scale might not be worth the additional computational effort imposed by ray tracing. Despite seismological studies, a comparison between the performance of straight-ray and curved-ray SWT at the near-surface scale is missing. In near-surface studies, the shot locations can be optimised to ensure that a high coverage of DCs can be achieved. This abundance of information facilitates shallow 2D or 3D characterisation with great details. Due to its ability to provide high lateral resolution, SWT has recently attracted the attention of researchers for near-surface studies, where high lateral heterogeneity is expected. Few researchers have used SWT for near-surface characterisation assuming straight-ray propagation of surface waves. Kugler et al. (2007) characterised shallow water marine sediments using Scholte waves dispersion data, Picozzi et al. (2009) applied SWT on high-frequency seismic noise data to construct a VS model up to 25 m in depth, Rector et al. (2015) employed SWT to obtain a VS model in a mining site, Ikeda and Tsuji (2020) successfully applied SWT in laterally heterogeneous media, Papadopoulou (2021) showed the applicability of SWT in near-surface characterisation in a mining site consisting of hard rocks and Khosro Anjom (2021) constructed a 3D VS model applying SWT on a large 3D dataset acquired for testing purposes in a mining area.

Since the level of complexity and lateral heterogeneity in the near surface is expected to be higher than in most seismological studies, the straight-ray approximation of surface waves may not be valid and curved-ray tomography should be used by means of ray tracing at each frequency. Fang et al. (2015) applied SWT on a shallow crustal study considering the effect of heterogeneity on wave propagation. They performed surface wave ray tracing at each frequency using a fast-marching method (Rawlinson and Sambridge, 2004). Wu et al. (2018) applied curved-ray SWT to obtain a shallow VS model at a mining site. Barone et al. (2021) applied different tomography methods, including eikonal tomography, to 3D active seismic data.

In curved-ray SWT, at each iteration a ray tracing method is applied at each frequency component to compute the ray path between the source and receivers. Even though this can increase the accuracy of the final model, it will lead to higher computational cost compared with straight-ray SWT. The computational efficiency is of great importance in seismic near-surface as, compared to seismological studies, the abundance of data at active seismic near-surface projects can significantly increase the computational cost. Therefore, it is necessary to investigate the gained improvement together with the associated additional computational cost from the curved-ray SWT over the straight-ray approach.

We apply straight-ray and curved-ray SWT on four datasets. Two examples include 3D synthetic models containing lateral velocity heterogeneity. We then apply SWT on two field datasets to evaluate the method on real data. For each dataset, 3D VS models from straight-ray and curved-ray SWT are obtained by direct inversion of DCs, and the accuracy and computational efficiency of the two approaches are compared.

In this section the applied methodology is described. Besides explaining the straight-ray and curved-ray SWT approaches and the differences between them, we also describe the employed procedure to optimise source positions and the process to estimate the DCs from the raw data.

## 2.1 Optimisation of source layout

For a given (random or regular) array configuration, we can optimise the locations of shots to ensure having high coverage DCs with minimum number of shots based on the guidelines by Da Col et al. (2020). In this approach, many shot positions are defined as the potential shot candidates. For each shot, we find all receiver pairs aligned with the shot. After computing all the possible receiver pairs for all the defined shot positions, the shots are sorted based on the number of in-line receiver pairs. Then we pick the shots which could provide the greatest number of unique pairs (i.e. potential DCs). If the data coverage is satisfactory also from the azimuthal point of view, we consider the selected shots as the final ones. Otherwise, more shots are added to increase the data coverage.

From the presented four examples in this study, the shot positions have been optimised for three examples (case studies 1–3). We also use a dataset (case study 4) where the acquisition layout mimics at a smaller scale the classical seismic exploration 3D cross-spread acquisition scheme with orthogonal lines of sources and receivers. This dataset, not being optimised (for a SWT study) will help in analysing the criticalities introduced by a non-optimal acquisition scheme.

## 2.2 Estimation of DCs

Once the acquisition layout is finalised, the DCs are estimated from the acquired data. We use a MATLAB code (Papadopoulou, 2021) that automatically retrieves the DCs between each receiver pair that are collinear with a source.

Here, we provide the general concepts based on which the code estimated the
DCs from the raw data (for detail see Papadopoulou, 2021). For each receiver
pair, a frequency domain narrow band-pass Gaussian filter, which was
originally proposed by Dziewonski and Hales (1972), is used to analyse the
traces into monochromatic components. The traces are then cross-correlated
frequency by frequency to produce the cross-correlation matrix. The phase
velocities of surface waves correspond to the maxima on the
cross-correlation matrix, but there are many maxima because in the
two-station method the observed phase delay is invariant under 2*π*
translation (Magrini et al., 2022). Hence, to avoid ambiguity in picking the
correct maxima, a reference DC is used. The reference DC is estimated
automatically using the multichannel analysis method (Park et al., 1998) for the
positions near to the receiver pair. The code picks all candidate DCs on
each cross-correlation matrix. Then, the candidate that is closest to the
reference DC at all frequencies is picked. Afterwards, a set of QC processes
allow data points to be rejected that do not follow the smooth trend of the DC and also poor quality DCs to be removed.

For the frequency band of the generic *i*th estimated DC, we put the
corresponding phase velocity values into a vector (*V*_{i}).
The input data for the inversion is a vector (*d*_{obs})
containing the phase velocities of all DCs as

where *N* is the total number of estimated DCs. The proposed equation by
Passeri (2019) is used to approximate the standard deviation (${\mathit{\sigma}}_{{V}_{j}})$ of the generic *j*th element of the phase velocity vector
(*V*_{j}) at its corresponding frequency (*f*_{j}) as

## 2.3 1D forward modelling

We carry out our experiments in a Cartesian coordinate system. The
subsurface is discretised into a set of 3D grid blocks where it is assumed
that the only unknown parameter of each grid block is the VS value while the Poisson ratio (*ν*) and density (*ρ*) are assumed to be known as a
priori information. Several 1D model points ** m** are defined. For each
model point, the local DC is computed using a Haskell (1953) and Thomson (1950) forward model modified by Dunkin (1965).

## 2.4 Computation of forward response

To obtain the forward response in the curved-ray SWT, first the ray path
between the generic receiver pair *R*_{1}–*R*_{2} for each frequency of the
DC should be computed. Having computed the phase velocities as a function
frequency at the position of each model point, the 2D phase slowness maps at
each frequency are built. Then, ray tracing (Noble et al., 2014) is
performed at every built phase velocity map to compute the frequency-dependent ray paths between the receiver pair (${l}_{{R}_{\mathrm{1}}{R}_{\mathrm{2}}})$.
The accuracy of the employed ray-tracing algorithm has already been
discussed by Noble et al. (2014). The frequency-dependent ray path between
the receiver pair is discretised to many points. At the generic *i*th
discretised point along the path, the phase slowness (*p*_{i}) is computed
using a bilinear interpolation among the computed local phase slowness
(inverse of phase velocity) values at the four surrounding model points as

where *x* and *y* show the position of each point. Figure 1 shows a schematic
representation of the bilinear interpolation along the discretised path
between the receiver pair.

The path-average phase slowness along the discretised path for each frequency (${p}_{{}_{{R}_{\mathrm{1}}{R}_{\mathrm{2}}}}\left(f\right))$ is then computed as

where *L* is the length of the interstation path and *N*_{p} represents
the number of discretised points along the path. The corresponding phase
velocity (${V}_{{}_{{R}_{\mathrm{1}}{R}_{\mathrm{2}}}}\left(f\right))$ is equal to the inverse
of the computed phase slowness.

We obtain the vector of the simulated DC for the receiver pair (*R*_{1}–*R*_{2})
by

where ${f}_{\mathrm{1}},\mathrm{\dots},{f}_{n}$ represent the frequency components of
the corresponding DC. It should be noted that each estimated DC may have a
frequency band different from the others. The vector of the forward response
of the model (** g**(m)), is then obtained as

## 2.5 Inversion algorithm

The employed inversion algorithm is based on the method proposed by Boiero (2009). We solve the inverse problem aiming at minimising the misfit function (Φ) which is defined as

where ** m** shows the vector of the model parameters,

*d*_{obs}is the observed data and

**(m) represents the forward response of the model that is computed from Eq. (6). The spatial regularisation matrix**

*g***R**

_{p}contains values of 1 and −1 for the constrained parameters and zeros elsewhere (see Auken and Christiansen, 2004, for details) and the extent of variation of each model parameter with respect to its neighbouring cells is controlled by the covariance matrix ${\mathbf{C}}_{{\mathbf{R}}_{\mathrm{p}}}$. To reduce the impact of spatial regularisation on the inversion results, in all four examples in this study, a large value (10

^{6}) is assigned to ${\mathbf{C}}_{{\mathbf{R}}_{\mathrm{p}}}$. The matrix

**C**

_{obs}consists of the uncertainties of the observed data and is obtained as

where *σ*_{V} is computed using Eq. (2). The defined
misfit function (Eq. 7) is minimised iteratively. At the *n*th
iteration, the current model *m*_{n} is updated as (Boiero,
2009):

where **G** is the sensitivity matrix of the data and *λ*
represents the damping factor (see Marquardt, 1963, for details). Two exit
criteria are defined to stop the inversion process. The inversion ends when
either the ratio of the values of the misfit function (Φ) from the
updated model and the current one (${\mathit{\lambda}}_{n+\mathrm{1}}/{\mathit{\lambda}}_{n})$ is
less than 1.0001 or the number of iterations exceeds 35.

To estimate the DCs from raw data, we have used the auto-picking code
(Papadopoulou, 2021) in which the DCs are sampled uniformly in frequency.
This means that each DC is non-uniformly sampled in terms of wavelength
which can drive the inversion algorithms to the shallowest part of the
subsurface without any significant updates in the deeper portion of the
initial velocity model (Khosro Anjom and Socco, 2019a). To address this
issue, a wavelength-based weighting scheme was applied in the inversion
process to compensate for this non-uniformity (see Khosro Anjom et al.,
2021, for details). Hence, the **C**_{obs} is modified as

where *σ*_{i,j} is the standard deviation of the *i*th data point
of the *j*th DC, and *w*_{i,j} is the corresponding weight that is
computed asthe

where Δ*λ*_{i,j} represents the wavelength difference between
the data point *i* of the *j*th DC and the data point with the smallest
wavelength distance from *i*, and Δ*λ*_{j,max} is the maximum
computed wavelength difference for the *j*th DC.

In this section, we apply straight-ray and curved-ray SWT approaches on four
datasets and compare the results. For each example, the straight-ray and
curved-ray SWT inversions start from the same initial model. Other inversion
parameters (${\mathbf{C}}_{{\mathbf{R}}_{\mathrm{p}}}$ and *λ*) are also the
same for the sake of comparison. It should be noted that only VS values are
updated during the inversion and the other parameters (*h*, *ν*, and *ρ*) are fixed. In case of synthetic examples, the true values of *ν*
and *ρ* are used in the inversion. For the field examples, *ν* and
*ρ* are approximated based on the available a priori information. Having
erroneous values of *ν* and *ρ* can induce errors in the inversion
results even though the sensitivity of surface waves to VS is more than *ν* (and far more than *ρ*).

## 3.1 Case study 1: the Blocky model

The Blocky model consists of a sequence of layers with vertically increasing velocity values, surrounding two blocks of velocity anomalies which extend 4 m in the horizontal and vertical directions (Fig. 2). The receivers are located in a regular grid with 1 m spacing in an area of 20 m ×20 m (Fig. 2a) and 16 shots (Fig. 2a) were chosen to generate the raw data after optimising the source positions (explained in Sect. 2.1). The synthetic data were generated using a 3D-finite difference (FD) code (SOFI3D software described in Bohlen, 2002) and no error has been added to the data. The code is an FD modelling programme based on the FD approach described by Virieux (1986) and Levander (1988) with some extensions. It can employ higher order FD operators, apply perfectly matched layer (PML) boundary conditions at the edges of the model, and it works in message passing interface (MPI) parallel environment which reduces the running time of the simulations. The used source is a function of the Ricker wavelet with a dominant frequency of 40 Hz. To avoid numerical dispersion, the minimum element size is defined in a way to have at least 8 grid points for the shortest wavelength to model the elastic waves propagation with the interpolation order of 4. To respect the wavelength sampling criteria, a mesh with an element size of 0.1 m (in horizontal and vertical dimensions) was defined. To ensure the stability of the simulation, the time stepping was set to $\mathrm{1.0}\times {\mathrm{10}}^{-\mathrm{5}}$ s to satisfy the Courant-Friedrichs-Lewy time stability condition. The geophysical parameters of the Blocky model are reported in Table 1.

The estimated 971 DCs are shown in Fig. 3a. The initial model for the
inversion is defined as a 5-layer 3D model where the thickness (*h*) of each
layer is fixed at 2 m. The horizontal dimensions of each inversion block are
2 m on the side and all blocks have an initial constant VS value of 200 m s^{−1}. The Poisson ratio (*ν*) and *ρ* values are assumed to be the same as the true model and are equal to 0.33 and 2000 kg m^{−3} in the whole subsurface, respectively. The same initial model is used as the starting model for
the SWT inversion in both straight-ray and curved-ray methods. The inversion
ends when the stopping criteria are satisfied. The values of the misfit
function at different iterations of the inversions are displayed in Fig. 3b.
The VS models at the last iteration of the inversion are displayed in Fig. 4.

Figure 4 shows that straight-ray and curved-ray SWT have modelled the location and the value of the high-velocity anomaly relatively accurately. The model from the curved-ray method is slightly superior at the grid blocks surrounding the high-velocity box (the black arrows in Fig. 4). In the case of a low-velocity anomaly, curved-ray SWT provided better results, since the bottom half of the low-velocity block is better resolved by the curved-ray approach (the white arrows in Fig. 4b and e). As shown in Table 4, the curved-ray approach produced slightly lower model misfit than straight-ray SWT.

## 3.2 Case study 2: the sand bar model

The sand bar model is designed to simulate a saturated environment where a sand layer is buried in unconsolidated clay. The model contains a curve-shaped high-velocity anomaly (the sand layer) embedded between two low-velocity clay layers (Fig. 6). The geophysical parameters of the sand bar model are shown in Table 2. The receivers are distributed at the surface as a regular grid with 2 m spacing (Fig. 5a). We defined sources at the same location of receivers and for each source we computed the aligned receiver pairs. Then, we picked 13 shots (Fig. 5a) which provided the highest data coverage to generate the synthetic data. The same finite difference code used for the Blocky model was used to obtain the sand bar synthetic dataset and no error was added to the synthetic data. The source is a function of Ricker wavelets with a dominant frequency of 40 Hz, and the minimum element size of the mesh grid was set to 0.1 m to prevent numerical dispersion. The time stepping was equal to $\mathrm{1.0}\times {\mathrm{10}}^{-\mathrm{5}}$ to avoid simulation instability.

The retrieved 1207 DCs are depicted in Fig. 6a. The defined initial model is
a 3D model with 10 layers of constant 1 m thickness where the VS values are
fixed at 80 m s^{−1}. The inversion blocks are 2 m in horizontal
dimensions. The initial Poisson ratio and density values are set equal to
the values of the true model (Table 2). The misfit function values at
different iterations of the inversion are shown in Fig. 6b. The SWT
inversion results for one horizontal and two vertical slices of the model
are shown in Fig. 7.

We can see in Fig. 7 that the VS models from both approaches are similar to each
other. Figure 7 shows that both methods have successfully located the
high-velocity anomaly. Not only are the velocity values close to the true
model (Fig. 5b to d) but the shape of the anomaly has also been clearly retrieved. The vertical slices at *X* (Fig. 7a and d) and *Y* directions (Fig. 7b
and e) do not display significant differences. The areas marked in dashed
black in the horizontal slices (Fig. 7c and f) show that the boundaries of
the anomaly are slightly clearer in the curved-ray approach (Fig. 7f) and
also the VS values in these areas are closer to the true VS value (Fig. 5d).

## 3.3 Case study 3: Pijnacker field

The data were acquired in a field near Pijnacker, South Holland, the Netherlands (Fig. 8a). An area of 27 m ×30 m was investigated by 120 geophones and 59 shot locations (Fig. 8b). The shot positions were optimised (Sect. 2.1) for the locations inside the array area and 15 shot locations which provided the highest coverage were chosen as the optimised shot positions. Moreover, 44 shot locations were chosen outside the acquisition area, each one at 3 m distance from every geophone located at the outer boundary of the acquisition area. The source was a vibrator that emitted a linear sweep signal from 2 to 100 Hz for 5 s at a force level of 1150 N. Some of the available shallow well data close to the field are depicted in Fig. 8c. They show that the field mainly consists of clay, together with peat and possibly sand in some locations. The extracted 972 DCs from the data are displayed in Fig. 8d.

Each inversion block extends 3 m horizontally. In this case the initial
model contains 6 layers where the layers get thicker with depth. The first
2 layers are 1 m thick, followed by 2 layers of 2 m and 2 of 3 m. The
initial model is defined regardless of the well information. The well data
are used later to assess the inversion results. The inversion started from
an initial VS value of 60 m s^{−1}. As the medium was (almost)
saturated, a high *ν* value (0.45) was chosen for the initial model. The
*ρ* values in the medium were assumed to be low (1700 kg m^{−3})
because it consisted of unconsolidated materials. The values of the initial
model parameters are reported in Table 3. The values of the misfit function
at different iterations are displayed in Fig. 9, and the SWT inversion
results for straight-ray and curved-ray methods are depicted in Fig. 10.

We can see in Fig. 10 that also in this case the VS models from the
straight-ray and curved-ray SWT are similar. The difference between the
horizontal slices (Fig. 10a and d) are clearer than the vertical ones. As
shown in the black dashes, the cells around the high velocity
portion have lower VS values in the curved-ray (Fig. 10d) than straight-ray SWT
(Fig. 10a). A previous 2D full waveform study (Bharadwaj et al., 2015) on a
clay field, which was not very far from the field location of our study,
obtained a VS model in the range of 40–80 m s^{−1} up to 15 m depth. This is
in agreement with the inversion results shown in Fig. 10. The high velocity
portions relate to the sand. It can be seen in the vertical slices in Fig. 10 that the depth of the high-velocity part (sand layer) is mainly in the range of
2–9 m, which seems reasonable given the a priori well data (Fig. 8c).

## 3.4 Case study 4: CNR field

The field data were acquired at the National Research Council (CNR) headquarters in Turin, Italy (Fig. 11a and b). The site consists of compacted sand and gravel formations surrounding an artificial loose sand body. The sand body occupies an area of 5 m ×5 m at the surface and the maximum depth reaches 2.5 m. The receiver layout consists of 4 lines which are 2.5 m apart. Each acquisition line includes 18 vertical 4.5 Hz geophones with 0.5 m spacing. The used source was an 8 kg hammer. The acquisition was carried out in 83 shot locations. Figure 11c shows the acquisition set-up which mimics a typical exploration 3D cross-spread acquisition scheme at a smaller scale. The estimated 315 DCs are shown in Fig. 11d.

The inversion started from an 8-layer 3D model where the horizontal and
vertical sizes of each grid are 0.5 m, VS is equal to 200 m s^{−1},
*ν* is approximated based on a previous study (Khosro Anjom et al.,
2019b) on the site and fixed at 0.33, and the density is fixed at 2000 kg m^{−3} as the site mainly consists of loose sand material. The misfit
function values at different iterations of the inversion are shown in Fig. 12. Both straight-ray and curved-ray SWT inversions started from the same
initial model and the results are presented in Fig. 13.

Figure 13 shows that the differences between straight-ray and curved-ray models are more pronounced in this example. There are some cells with relatively high-velocity values inside the sand body in the model obtained from the straight-ray SWT (Fig. 13a). The boundaries of the loose sand body at the surface are better retrieved by the curved-ray SWT (Fig. 10d). The areas shown in white dashes in Fig. 13b and e show that the gradual increase of the VS values with depth inside the sand body is clearer in the model from the curved-ray SWT(Fig. 13e). The black arrow in Fig. 13c shows the high-velocity cells inside the loose sand body in the retrieved model from the straight-ray SWT. The reason is that in this area (close to the interface of the sand body and the background medium) the assumed paths in the straight-ray approach are much shorter than the true paths and therefore the obtained VS from the inversion becomes unrealistically high. This artefact does not exist in the corresponding slice from the curved-ray SWT (Fig. 13f).

We have applied straight-ray and curved-ray SWT to four datasets and compared the results. In this section, we investigate the results in more detail considering ray paths, data weighting, models and data misfits, and computational cost.

## 4.1 Ray paths

The improvement of the model obtained by the curved-ray SWT compared to straight-ray SWT, particularly at the boundaries of velocity anomalies, has been shown in the synthetic and real world examples. Some selected examples of the computed ray paths at the last iteration of the curved-ray SWT are depicted in Fig. 14.

In all the three models in Fig. 14 the receivers A and B are located outside the velocity anomalies, and we see that the computed ray paths between them do not cross the anomalies. Therefore, the obtained paths do not deviate considerably from a straight line. In Fig. 14a, the high-velocity anomaly exists at the depth range of 3–6 m. Hence, we can see that the high-frequency components of the DCs, which correspond to the shallow parts of the model, do not deviate from a straight line; however, the lower frequencies (i.e. higher wavelengths) for the C-D and G-H pairs have deviated from a straight line and travelled through the high-velocity parts. In Fig. 14b, the depth of velocity anomalies is in the range of 2–6 m. We see that also in this case the ray paths for higher frequencies have almost no deviations from a straight line as they do not cross the anomalies. However, we can see for the obtained paths between B-C and D-E pairs that the lower frequencies have bypassed the low-velocity anomaly. Similarly, lower frequencies in the case of the G-F pair have deviated from a straight path and travelled through the high-velocity anomaly. In Fig. 14c, the sand body (low-velocity anomaly) starts at the surface and reaches a maximum depth of 2.5 m. Its area shrinks from 5 m ×5 m at the surface to 3 m ×3 m at a depth of 2.5 m . The shrinkage in size of the anomaly can be seen in the computed path for the B-G, C-D, and E-F pairs, where the degree of the deviation from the straight line decreases as the depth increases (frequency decreases).

Even though the exact boundaries of the anomaly (sand layer) are unknown for the Pijnacker field, the computed ray paths can provide helpful insights. For instance, the computed ray paths from straight-ray and curved-ray SWT, for the DCs data with the wavelengths in the range of 6–9 m are displayed in Fig. 15.

As the initial VS model is vertically and horizontally homogeneous, the initial ray paths for both straight-ray and curved-ray SWT are straight lines. As shown in Fig. 15a, the ray paths do not change during the inversion in the straight-ray approach. However, the paths are updated at every iteration of the curved-ray SWT inversion. We see that some areas in Fig. 15b (shown in dashed red) are bypassed by almost all the rays even though the data coverage of these areas in the straight-ray approach (Fig. 15a) is considerably higher. Therefore, these portions correspond to the low-velocity materials, i.e. clay and peat. The area between these low-velocity portions has both a higher concentration of ray paths and higher average phase velocity values. Therefore, they probably show the sand layer. These locations agree with the obtained VS model from the curved-ray SWT inversion (Fig. 10d).

## 4.2 Misfits and computational costs

We have shown the inversion results from the straight-ray and curved-ray
SWT. In this part, we compare the results quantitatively. We carried out the
inversions on 40 cores on a cluster with the processor type of
Intel^{®} Xeon^{®} E5-2650 v3. In Table 4, we report
the number of iterations (*n*_{i}), the running time (*r*_{t}), the maximum
memory consumption during the inversion process (mem_{max}), the relative
data misfit at the last iteration of the inversion (*e*_{d}), the relative
model misfit for all cells (*e*_{m}) and only the ones in the depth range of
the target (*e*_{t}), and the cost of inversion to be run at Microsoft cloud
service.

We define the relative data misfit (*e*_{d}) as

where *d*_{obs} is the vector of the experimental DCs and
fw(*m*_{final}) represents the computed
forward response of the model at the final iteration of the inversion. In the
case of the synthetic examples (the Blocky and sand bar models), we can
compare the obtained VS models from the inversion (VS_{final}) with the true model (VS_{true}). We compute the average
relative model misfit (*e*_{m}) as

For each parameter in Table 4, the last column shows the relative difference
between the curved-ray and straight-ray approaches (*d*_{CR−SR}) that has
been computed as

where *a*_{CR,j} and *a*_{SR,j} are the values of each parameter from
curved-ray and straight-ray approaches, respectively, and *J* is the number of
examples for which there is an existing value for that parameter.

We can see in Table 4 that in all examples except for the Blocky model, the
curved-ray SWT has converged in less iterations than the straight-ray SWT.
However, the curved-ray SWT has increased *r*_{t} by 25 % compared to the
straight-ray SWT. For all the case studies, the curved-ray SWT needed more memory
(11 % by average) than the straight-ray SWT. In terms of data misfit (*e*_{d}), the
straight-ray approach provided better performance than the curved-ray approach.
We can also see that the difference between the obtained *e*_{d} values
from the straight-ray and curved-ray SWT is negligible in the case of the synthetic
examples (the sand bar and Blocky models), but the difference is more
pronounced for the field examples (the CNR and Pijnacker). Despite having a higher *e*_{d}, the curved-ray approach produced lower model misfits than the straight-ray approach. Using curved-ray SWT decreased the overall model misfit
(*e*_{m}) and the target model misfit (*e*_{t}) by 2 % and 4 %,
respectively. Finally, we see in Table 4 that using curved-ray SWT has
increased the computational cost by an average of 25 %.

## 4.3 Impact of the data coverage

In all the examples presented, the computed VS models from the straight-ray and curved-ray SWT do not differ significantly except for the CNR field. Since the source positions had not been optimised in this example, the DCs coverage is low, particularly in the shallower portion of the medium. Figure 16 depicts the ray paths of the DCs data with the wavelengths in the range of 0–1 m.

We can see in Fig. 16a that some areas of the medium are not covered with straight rays, especially outside the sand body. It should be noted that for both cases, the ray paths at the first iteration are straight lines as the initial model has a constant VS value for all cells. However, in the curved-ray approach (Fig. 16b) the ray paths are flexible and can adjust to the updated subsurface velocity during the inversion process. Figure 16b also shows that the ray paths responded properly to the edges of the loose sand body, travelling through the faster part of the model.

## 4.4 Weighting effect

As mentioned previously, uneven sampling of DC data in terms of wavelength can be problematic in SWT inversion. For instance, most of the extracted DC data (81 %) of the Pijnacker field have wavelengths less than 3 m while the available well data from the area suggest that the depth of the target is expected to vary in the range of 2–7 m. This can be a serious problem as the inversion might reach the defined stopping criteria without any significant updates in the deeper portion of the initial velocity model. Figure 17 shows the obtained VS models with (Fig. 17a and b) and without (Fig. 17c and d) the wavelength-based weighting at 5.5 m depth.

In Fig. 17, we can see the improvement of the model after applying the wavelength-based weighting method (Fig. 17a and b) compared with the non-weighted model (Fig. 17c and d) where the non-weighted inversions have barely retrieved any pattern to model the target (sand layer).

## 4.5 Comparison with previous studies

We have shown that optimisation of source positions can provide higher data coverage than a typical 3D cross-spread acquisition scheme. We have evaluated straight-ray and curved-ray SWT at the near-surface scale and a comparison of our results might not necessarily agree with previous (global or regional scale) seismological studies. For instance, Spetzler et al. (2001) pointed out that the maximum deviations of ray paths from a straight line is mostly below the estimated resolution. However, we have shown that the deviation from a straight line can be resolved at the near-surface scale (Fig. 14). We also showed that in the case of low data coverage, using the curved-ray approach significantly improves the obtained VS model. This result might not agree completely with the result of the (seismological) study by Trampert and Spetzler (2006), where they pointed out that increasing the data coverage is the main factor to increase the resolution of the model. Our results show that in the case of high data coverage, the model improvement achieved in the curved-ray approach may not be worth the additional computational effort, which agrees with the results of the study by Bozdag and Trampert (2008).

We applied SWT to four datasets and built near-surface VS models. We compared the obtained results from the straight-ray and curved-ray SWT in terms of data misfit, model misfit, and computational cost. We showed that compared to the straight-ray approach, using curved-ray SWT improves the accuracy of the computed VS model. We illustrated that the acquisition layout can play an important role in the data coverage obtained and consequently in the inversion results. We showed that the classical cross-spread acquisition layout (which was used in the CNR example) may not provide high DC coverage. In this case, the improvement of inversion results from the curved-ray SWT can be significant. We also showed that in the case of high data coverage, which can be achieved by optimisation of source positions, the difference between the obtained VS models from the straight-ray and curved-ray approaches can be very small even in the presence of high lateral variation of the velocity.

The data can be made available by contacting the corresponding author. The code can also be made available by contacting the corresponding author after carrying out some additional work to make it user-friendly.

MK worked on the processing and inversion of all the datasets, with coordination and supervision of ES and LVS. MK and ES contributed to seismic data acquisition in Pijancker field and LVS coordinated the seismic data acquisition in the CNR site. MK wrote the original paper draft, with contributions from all the authors.

The contact author has declared that none of the authors has any competing interests.

Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

We would like to thank Seismic Mechatronics for providing the vibrator source, CNR group for giving access to data acquisition, Compagnia di San Paolo for funding the PhD of Mohammadkarim Karimpour, and all the people involved in data acquisition.

This paper was edited by Ulrike Werban and reviewed by Emanuel Kästle, Fabrizio Magrini, and one anonymous referee.

Auken, E. and Christiansen, A. V.: Layered and laterally constrained 2D inversion of resistivity data, Geophysics, 69, 752–761, https://doi.org/10.1190/1.1759461, 2004.

Barone, I., Kästle, E., Strobbia, C., and Cassiani, G.: Surface wave tomography using 3D active-source seismic data, Geophysics, 86, EN13–EN26, https://doi.org/10.1190/GEO2020-0068.1, 2021.

Bharadwaj, P., Mulder, W. A., Drijkoningen, G. G., and Reijnen, R.: Looking Ahead of a Tunnel Boring Machine with 2-D SH Full Waveform Inversion, 77th EAGE Conference and Exhibition, Madrid, Spain, June 2015, 1–5, https://doi.org/10.3997/2214-4609.201412803, 2015.

Bohlen, T.: Parallel 3-D viscoelastic finite-difference seismic modelling, Comput. Geosci., 28, 887–899, https://doi.org/10.1016/S0098-3004(02)00006-7, 2002.

Boiero, D.: Surface wave analysis for building shear wave velocity models, PhD thesis, Politecnico di Torino, https://www.researchgate.net/profile/Daniele-Boiero/publications (last access: 19 October 2022), 2009.

Boschi, L. and Dziewonski, A. M.: High- and low-resolution images of the Earth's mantle: Implications of different approaches to tomographic modelling, J. Geophys. Res, 104, 25567–25594, https://doi.org/10.1029/1999JB900166, 1999.

Boschi, L. and Ekström, G.: New images of the Earth's upper mantle from measurements of surface wave phase velocity anomalies, J. Geophys. Res.-Sol. Ea., 107, 1–14, https://doi.org/10.1029/2000JB000059, 2002.

Bozdag, E. and Trampert, J.: On crustal corrections in surface wave tomography, Geophys. J. Int., 172, 1066–1082, https://doi.org/10.1111/j.1365-246X.2007.03690.x, 2008.

Bussat, S. and Kugler, S.: Offshore ambient-noise surface-wave tomography above 0.1 Hz and its applications, Lead. Edge, 30, 514–524, https://doi.org/10.1190/1.3589107, 2011.

Da Col, F., Papadopoulou, M., Koivisto, E., Sito, L., Savolainen, M., and Socco, L. V.: Application of surface-wave tomography to mineral exploration: a case study from Siilinjärvi, Finland, Geophys. Prospect., 68, 254–269, https://doi.org/10.1111/1365-2478.12903, 2020.

Dunkin, J. W.: Computation of modal solutions in layerered, elastic mida at high frequencies, Bull. Seismol. Soc. Am., 55, 335–358, 1965.

Dziewonski, A. M. and Hales, A. L.: Numerical Analysis of Dispersed Seismic Waves, Methods in Computational Physics: Advances in Research and Applications, 11, 39–85, https://doi.org/10.1016/B978-0-12-460811-5.50007-6, 1972.

Ekstrom, G., Tromp, J., and Larson, E. W. F.: Measurements and global models of surface wave propagation: J. Geophys. Res., 102, 8137–8157, https://doi.org/10.1029/96JB03729, 1997.

Fang, H., Yao, H., Zhang, H., Huang, Y., and van der Hilst, R. D.: Direct inversion of surface wave dispersion for three-dimensional shallow crustal structure based on ray tracing: methodology and application, Geophys. J. Int., 201, 1251–1263, https://doi.org/10.1093/gji/ggv080, 2015.

Haskell, N.: The dispersion of surface waves on multilayered media, Bul. Seimol. Soc. Am., 43, 17–34, https://doi.org/10.1785/BSSA0430010017, 1953.

Ikeda, T. and Tsuji, T.: Two-station continuous wavelet transform cross-coherence analysis for surface-wave tomography using active-source seismic data, Geophysics, 85, EN17–EN28, https://doi.org/10.1190/geo2019-0054.1, 2020.

Kästle, E. D., El-Sharkawy, A., Boschi, L., Meier, T., Rosenberg, C., Bellahsen, N., Cristiano, L., and Weidle, C.: Surface wave tomography of the Alps using ambient-noise and earthquake phase velocity measurements, J. Geophys. Res.-Sol. Ea., 123, 1770–1792, https://doi.org/10.1002/2017JB014698, 2018.

Khosro Anjom, F.: S-wave and P-wave velocity model estimation from surface waves, PhD thesis, Politecnico di Torino, http://hdl.handle.net/11583/2912984 (last access: 19 October 2022), 2021.

Khosro Anjom, F., and Socco, L. V.: Improved surface wave tomography: Imposing wavelength-based weights, Extended Abstracts, 38th GNGTS national convention, Rome, 12–14 November 2019, 681–684, https://gngts.ogs.it/archivio/index.php/2019-xxxviii-rm (last access: 19 October 2022), 2019a.

Khosro Anjom F., Teodor, D., Comina, C., Brossier, R., Virieux, J., Socco L. V.: Full waveform matching of VP and VS models from surface waves, Geophys. J. Int., 218, 1873–1891, https://doi.org/10.1093/gji/ggz279, 2019b.

Khosro Anjom, F., Browaeys, T. J., and Socco, L. V.: Multi-modal surface wave tomography to obtain S- and P-wave velocities applied to the recordings of UAV deployed sensors, Geophysics, 86, 399–412, https://doi.org/10.1190/geo2020-0703.1, 2021.

Kugler, S., Bohlen, T., Forbriger, T., Bussat, S., and Klein, G.: Scholte-wave tomography for shallow-water marine sediments, Geophys. J. Int., 168, 551–570, https://doi.org/10.1111/j.1365-246X.2006.03233.x, 2007.

Laske, G.: Global observations of off-great-circle propagation of long-period surface waves, Geophys. J. Int., 13, 245–259, https://doi.org/10.1111/j.1365-246X.1995.tb06673.x, 1995.

Levander, A. R.: Fourth-order finite-difference P-SV seismograms, Geophysics, 53, 1425–1436, https://doi.org/10.1190/1.1442422, 1988.

Levshin, A. L., Barmin, M. P., Ritzwoller, M. H., and Trampert, J.: Minor-arc and major-arc global surface wave diffraction tomography, Phys. Earth Planet. Inter., 149, 205–223, https://doi.org/10.1016/j.pepi.2004.10.006, 2005.

Lin, F.-C., Moschetti, M. P., and Ritzwoller, M. H.: Surface wave tomography of the western United States from ambient seismic noise: Rayleigh and Love wave phase velocity maps, Geophys. J. Int., 173, 281–298, https://doi.org/10.1111/j.1365-246X.2008.03720.x, 2008.

Lin, F.-C., Ritzwoller, M. H., and Snieder, R.: Eikonal tomography: Surface wave tomography by phase front tracking across a regional broad-band seismic array, Geophys. J. Int., 177, 1091–1110, https://doi.org/10.1111/j.1365-246X.2009.04105.x, 2009.

Magrini, F., Lauro, S., Kästle, E., and Boschi, L.: Surface-wave tomography using SeisLib: a Python package for multiscale seismic imaging, Geophys. J. Int., 231, 1011–1030, https://doi.org/10.1093/gji/ggac236, 2022.

Marquardt, D. W.: An algorithm for least squares estimation of nonlinear parameters, Journal of the Society of Industrial Applied Mathematics, 11, 431–441, https://doi.org/10.1137/0111030, 1963.

Noble, M., Gesret, A., and Belayouni, N.: Accurate 3-D finite difference computation of traveltimes in strongly heterogeneous media, Geophys. J. Int., 199, 1572–1585, https://doi.org/10.1093/gji/ggu358, 2014.

Papadopoulou, M.: Surface wave methods for mineral exploration, PhD thesis, Politecnico di Torino, http://hdl.handle.net/11583/2914550 (last access: 19 October 2022), 2021.

Park, C. B., Miller, R. D., and Xia, J.: Imaging dispersion curves of surface waves on multi-channel record, SEG Technical Program Expanded Abstracts, 1377–1380, https://doi.org/10.1190/1.1820161, 1998.

Passeri, F.: Development of an advanced geostatistical model for shear wave velocity profiles to manage uncertainties and variabilities in ground response analyses, PhD thesis, Politecnico di Torino, http://hdl.handle.net/11583/2730182 (last access: 19 October 2022), 2019.

Passier, M. L., Van der Hilst, R. D., and Snieder, R. K.: Surface wave waveform inversions for local shear-wave velocities under eastern Australia, Geophys. Res. Lett., 24, 1291–1294, https://doi.org/10.1029/97GL01272, 1997.

Picozzi, M., Parolai, S., Bindi, D., and Strollo, A.: Characterization of shallow geology by high-frequency seismic noise tomography, Geophys. J. Int., 176, 164–174, https://doi.org/10.1111/j.1365-246X.2008.03966.x, 2009.

Rawlinson, N. and Sambridge, M.: Wave front evolution in strongly heterogeneous layered media using the fast marching method, Geophys. J. Int., 156, 631–647, https://doi.org/10.1111/j.1365-246X.2004.02153.x, 2004.

Rector, J. W., Pfeiffe, J., Hodges, S., Kingman, J., and Sprott, E.: Tomographic imaging of surface waves: A case study from the Phoenix Mine, Battle Mountain, Nevada, Lead. Edge, 34, 1360–1364, https://doi.org/10.1190/tle34111360.1, 2015.

Ritzwoller, M. H. and Levshin, A. L.: Eurasian surface wave tomography: Group velocities, J. Geophys. Res.-Sol. Ea., 103, 4839–4878, https://doi.org/10.1029/97JB02622, 1998.

Ritzwoller, M. H., Shapiro, N. M., Barmin, M. P., and Levshin, A. L.: Global surface wave diffraction tomography, J. Geophys. Res., 107, 2335, https://doi.org/10.1029/2002JB001777, 2002.

Shapiro, N. M., Ritzwoller, M. H., Molnar, P. and Levin, V.: Thinning and flow of Tibetan crust constrained by seismic anisotropy, Science, 305, 233–236, https://doi.org/10.1126/science.1098276, 2004.

Sieminski, A., Lévêque, J.-J., and Debayle, E.: Can finite-frequency effects be accounted for in ray theory surface wave tomography?, Geophys. Res. Lett., 31, L24614, https://doi.org/10.1029/2004GL021402, 2004.

Simons, F. J., Zielhuis, A., and van der Hilst, R. D.: The deep structure of the Australian continent from surface wave tomography, Develop. Geotect., 24, 17–43, https://doi.org/10.1016/S0419-0254(99)80003-2, 1999.

Spetzler, J., Trampert, J., and Snieder, R.: Are we exceeding the limits of the great circle approximation in global surface wave tomography?, Geophys. Res. Lett., 28, 2341–2344, https://doi.org/10.1029/2000GL012691, 2001.

Spetzler, J., Trampert, J., and Snieder, R.: The effect of scattering in surface wave tomography, Geophys. J. Int., 149, 755–767, https://doi.org/10.1046/j.1365-246X.2002.01683.x, 2002.

Thomson, W. T.: Transmission of elastic waves through a stratified solid medium, J. Appl. Geophys., 21, 89–93, https://doi.org/10.1063/1.1699629, 1950.

Trampert, J. and Spetzler, J.: Surface wave tomography: finite-frequency effects lost in the null space, Gephys. J. Int., 164, 394–400, https://doi.org/10.1111/j.1365-246X.2006.02864.x, 2006.

Trampert, J. and Woodhouse, J. H.: Global phase velocity maps of Love and Rayleigh waves between 40 and 150 seconds, Gephys. J. Int., 122, 675–690, https://doi.org/10.1111/j.1365-246X.1995.tb07019.x, 1995.

Van Heijst, H. J. and Woodhouse, J.: Global high-resolution phase velocity distributions of overtone and fundamental-mode surface waves determined by mode branch stripping, Geophys. J. Int., 137, 601–620, https://doi.org/10.1046/j.1365-246x.1999.00825.x, 1999.

Virieux, J.: SH-wave propagation in heterogeneous media: velocity-stress finite-difference method, Geophys., 51, 889–901, https://doi.org/10.1071/EG984265a, 1986.

Woodhouse, J. H. and Dziewonski, A. M.: Mapping the upper mantle: three-dimensional modelling of Earth structure by inversion of seismic waveforms, J. Geophys. Res.-Sol. Ea., 89, 5953–5986, https://doi.org/10.1029/JB089iB07p05953, 1984.

Wu, Z. and Rector, J.: Seismic-velocity inversion using surface-wave tomography, SEG Technical Program Expanded Abstracts, 2612–2616, https://doi.org/10.1190/segam2018-2998108.1, 2018.

Yao, H., Beghein, C., and van der Hilst, R. D.: Surface wave array tomography in SE Tibet from ambient seismic noise and two-station analysis – II. Crustal and upper-mantle structure, Geophys. J. Int., 173, 205–219, https://doi.org/10.1111/j.1365-246X.2007.03696.x, 2008.

Yao, H., van der Hilst, R. D., and Montagner, J.-P.: Heterogeneity and anisotropy of the lithosphere of SE Tibet from surface wave array tomography, J. Geophys. Res.-Sol. Ea., 115, B12, https://doi.org/10.1029/2009JB007142, 2010.

Yoshizawa, K. and Kennett, B. L. N.: Multimode surface wave tomography for the Australian region using a three-stage approach incorporating finite frequency effects, J. Geophys. Res.-Sol. Ea., 109, B02310, https://doi.org/10.1029/2002JB002254, 2004.

Zhou, Y., Dahlen, F. A., Nolet, G., and Laske, G.: Finite-frequency effects in global surface-wave tomography, Geophys. J. Int., 163, 1087–1111, https://doi.org/10.1111/j.1365-246X.2005.02780.x, 2005.