- Open Access
Forecasting volcanic ash deposition using HYSPLIT
© The Author(s). 2017
- Received: 15 September 2016
- Accepted: 22 February 2017
- Published: 4 March 2017
A major source of error in forecasting where airborne volcanic ash will travel and land is the wind pattern above and around the volcano. GNS Science, in conjunction with MetService, is seeking to move its routine ash forecasts from using the ASHFALL program, which cannot allow for horizontal variations in the wind pattern, to HYSPLIT, which uses a full 4-D atmospheric model. This has required some extensions to the standard version of the HYSPLIT program, both to get appropriate source terms and to handle the fall velocities of ash particles larger than 100 microns.
Application of the modified HYSPLIT to ash from the Te Maari eruption of 6 August 2012 from Tongariro volcano gives results similar to the observed ash distribution. However, it was also apparent that the high precision of these results could be misleading in actual forecasting situations, and there needs to be ways in which the likely errors in atmospheric model winds can be incorporated into ash models, to show all the areas in which there is a significant likelihood of deposited ash with each particular volcanic eruption model.
- Volcanic hazard
- Volcanic ash
- Atmospheric models
- Mt Tongariro
- Te Maari
The standard eruption model input parameters used in New Zealand by GNS Science, with three volumes and two column heights for each volcano
column height (high) km ASL
column height (low) km ASL
tephra volume large km3
tephra volume medium km3
tephra volume small km3
ash size distribution
These forecasts are currently produced by the program ASHFALL, originally described in Hurst (1994), which is now somewhat out-dated. ASHFALL follows the ash particles from an initial vertical eruption column as they are moved horizontally by the wind, and at the same time fall vertically with a velocity which depends on their size and density. It was designed to have a minimal processing requirement, based on the processing power of mid-1990s Personal Computers. To obtain reduced processing times, ASHFALL ignored vertical diffusion of the ash, although its effect was partly accounted for by using a large value for the horizontal diffusion coefficient. This horizontal diffusion coefficient is effectively a “fudge factor”, which spreads out the expected ash distribution to incorporate uncertainties in the wind pattern and other parameters. ASHFALL uses MetService (New Zealand Meteorological Service) forecasts of the wind at various levels above each volcano. However, it does not allow for any horizontal variations in the wind pattern, i.e. ASHFALL can only use 1-D spatial wind fields, although it does allow for wind changes with time.
Hurst and Turner (1999) found that the forecast wind field was the major source of error in the volcanic ash distribution from Ruapehu eruptions. During investigations as to how the wind information used by ASHFALL might be improved, we looked at the atmospheric dispersion model HYSPLIT (Stein et al., 2015), already in use by MetService for the movement of fine particles travelling in the atmosphere, such as volcanic ash, and found it has the capability for estimating the distribution of ash particles on the ground. As well as capturing the influence of realistic atmospheric motion in ash transport, HYSPLIT can also model in-cloud (rainout) and below-cloud (washout) wet deposition processes.
HYSPLIT is a hybrid Lagrangian dispersion model, developed by NOAA/ARL which is used by MetService, in its role as a Volcanic Ash Advisory Centre (VAAC), to model airborne volcanic ash, with meteorological data provided by external and in-house NWP (Numerical Weather Prediction) models, which operate with 3 spatial dimensions and time. The spatial resolution of these models is 4 km, and the temporal resolution one hour. HYSPLIT is operationally used by several of the 9 Volcanic Ash Advisory Centres for aviation forecasting. A by-product of the HYSPLIT volcanic ash dispersion simulations is the ash deposition at the ground surface. The ground surface elevation is modelled at the same resolution as the atmospheric model. Aside from the dispersion of volcanic ash, HYSPLIT is used in several other atmospheric transport applications, including the dispersion of hazardous materials (e.g. nuclear material after the Fukushima reactor accident), air quality modelling (e.g. ozone, visibility, haze, and dioxin), dust storms, smoke, and the transport of biological material (e.g. pollen and mould spores) (Stein et al., 2015). Rather than using a horizontal dispersion coefficient, the dispersion was calculated from the friction velocity, height and boundary layer height following Kantha and Clayson (2000), where there are different equations for stable/neutral and unstable layers for both the surface and boundary layer. Above the boundary layer a mixing coefficient obtained from mixing length theory is used to calculate the velocity variances (Draxler and Hess, 1997).
We initially compared the ash deposition results from HYSPLIT with ASHFALL for similar eruptions and wind patterns. This showed that alterations to the standard fall velocity model of HYSPLIT were required to deal with ash particles larger than about 100 microns, which make up the bulk of ash deposits near a volcano. This is not a consideration in the aviation applications of HYSPLIT, as these particles are the ones that rapidly fall out of ash clouds.
Ash sizes and fall velocities
HYSPLIT was originally designed to use atmospheric models to calculate the tracks of pollutants in the atmosphere (Stein et al., 2015). In regard to volcanic ash, it is used for tracking the small ash particles with long residence times that are hazardous to aircraft generally at considerable distances from the volcano. Accordingly by default it only considers ash particles less than 100 microns in diameter (e.g. in VAFTAD, Heffter and Stunder (1993)). The terminal velocity for these small particles can be calculated by Stokes Law, which applies in the laminar flow region, with Reynolds Number less than 0.4.
Aggregation of ash particles can have significant effects on ash distribution (Carey and Sigurdsson, 1982, Mastin et al., 2016), however this is not considered in either HYSPLIT or ASHFALL, and the focus of this work is the incorporation of realistic wind fields.
The larger (>100 micron) ash particles fall at higher terminal velocities, which produce turbulent air flow, with Reynolds Numbers greater than 500, and their actual terminal velocities are much less than that given by Stokes Law (Rose, 1993). Volcanologists typically use empirical methods or a range of equations for particles of different sizes, based on the Reynolds Number (Bonadonna et al., 1998). Figure 1 also shows how the three equations used for different ash sizes by Bonadonna et al. (1998) can all be matched by an equation derived by Ganser (1993) covering all particle sizes. This Ganser equation has recently been incorporated in HYSPLIT (Dare, 2015) and we have used this in our ash modelling.
Accordingly, we have started the implementation of routine ash forecasts from HYSPLIT, using the same ten volcanoes, three sizes of eruptions, and two eruption column heights as we use for ASHFALL.
Ash distribution comparisons for Te Maari eruption of 6 August 2012
We did not compare a HYSPLIT model with the actual volcanic ash thicknesses from the 1995 and 1996 eruptions of Ruapehu, used to evaluate the performance of ASHFALL predictions by Hurst and Turner (1999), because of the difficulty in obtaining an accurate 4 dimensional wind data for that time. However, there was a small ash eruption from the Upper Te Maari crater of Mt Tongariro on 6 August 2012, and NWP data for this date was archived by MetService, making it comparatively easy to calculate a hindcast for this event with HYSPLIT and ASHFALL. This NWP data was from the operational 8 km resolution WRF-ARW model, using European Centre for Medium Range Weather Forecasting (ECMWF) Integrated Forecasting System (IFS) data for initial and boundary conditions.
Because relevant atmospheric model data had been archived, it was comparatively easy to run HYSPLIT with the same information for the Te Maari eruption as would be available for an eruption today. The results have been compared with the main plume that travelled eastwards. Some ash travelled north from Te Maari, but it was clear (Lube et al., 2014; Pardo et al., 2014; Turner et al., 2014) that these ash deposits were produced by low-angle directed blasts.
The initial result from the HYSPLIT model with a point ash source had an extremely narrow ash plume heading east. With such a narrow plume we need to take account of the horizontal extent of the umbrella portion of the initial eruption column, as the width of this will significantly affect the near-source ash distribution. This has not been necessary with ASHFALL, because of the large horizontal diffusion coefficient it used. The GNS webcam south of Ruapehu, with an infra-red sensitive camera which observed the top portion of the Te Maari eruption column (Crouch et al., 2014), suggested a diameter of the initial eruption column of approximately 1.5 km, so we modelled the initial ash distribution as a vertical cylinder with this diameter, with uniform ash concentration horizontally, and a Suzuki distribution vertically. This technique was used by Crawford et al. (2016), but on a much larger scale, when modelling the 2008 eruption of Kasatochi. It was also apparent from the radar images in Crouch et al., (2014) that the eruption column was not vertical, but directed northwards, with its top region between one and two kilometres north of the source vent. We did not try to model a sloping column, but since most of the ash is in the top region of the column, we simply shifted the source one kilometre north of the Upper Te Maari crater.
The ash distribution predicted by ASHFALL for the Te Maari eruption has already been discussed by (Turner et al., 2014), which also compared both the ground and satellite measurements of where ash particles travelled with the results of the UK Met Office aerial dispersion model NAME-III (Jones, 2004), which used the NWP model NZLAM-12. The NAME and HYSPLIT models are very similar; both being Lagrangian dispersion models employed for a range of atmospheric pollution problems. NAME-III and HYSPLIT gave fairly similar ash distributions from this eruption, and in particular both had narrow ash plumes compared to ASHFALL. We will not discuss the differences between the ash distributions from these modelling programs further, other than to note that they probably are as much due to using different atmospheric models as to differences between the programs.
The region further downwind from this eruption was mountainous and virtually unpopulated until at least 80 km from Te Maari, and by then only trace amounts of volcanic ash were present, so all that could be said was that it was present or not present. Figure 6 shows which of the small settlements from 80 to 200 km reported either the presence or absence of ash. We have compared these reports to the outer limits of the ASHFALL and HYSPLIT predictions, effectively for an ash thickness of a few microns.
In Fig. 6 it can be seen that the narrow range of ash directions predicted by HYSPLIT does not cover all the places where ash was observed, suggesting that the wind was directed slightly more to the north than predicted by the atmospheric model. The available ground truth data in the far downwind area is too limited to let us distinguish between the narrow ash distribution of the HYSPLIT model and the much wider distribution from ASHFALL. However, the narrowness of the ash distribution in the near-source region does suggest that we have a narrow plume, but directed slightly north of where the atmospheric model used for HYSPLIT predicted it to be.
The ash predictions produced by HYSPLIT from a 4-D atmospheric model use much more information about the atmospheric wind pattern, and so are potentially much more accurate than the ASHFALL model that is currently used which assumes a horizontally uniform wind profile. For the 6 August 2012 eruption from the Upper Te Maari crater of Tongariro, the HYSPLIT forecast using an archived atmospheric model agreed well with the actual ash distribution recorded about 12 km downwind. There was not such good agreement between HYSPLIT and the reports of where small amounts of ash were present in areas over 80 km downwind. As found by Hurst and Turner (1999) for the 1995 and 1996 eruptions of Ruapehu, the main reason for the difference between forecast and actual ash distributions was the difference between the forecast and actual wind pattern.
HYSPLIT should provide a much better match to the ash distribution of an actual eruption than ASHFALL, because of the more detailed atmospheric model, and because it more completely accounts for ash removal processes (e.g. wet deposition). However, when using these programs for forecasting purposes, there are two factors that need to be considered. Firstly, HYSPLIT outputs have more detail, compared to the simple ellipses produced by ASHFALL, so they give a higher impression of accuracy. Secondly, without the non-physically large horizontal diffusion coefficient used in ASHFALL, HYSPLIT sometimes forecasts narrow ash distributions, as was seen for the Te Maari eruption, for which a very small change in wind direction will displace the forecast ashfall area to the extent that it no longer overlaps with the actual ashfall area some distance from the vent. This difficulty in demonstrating value in more detailed forecasts is something already encountered in NWP for normal weather forecasts, where for instance high resolution forecasts of severe convection are seen subjectively as being more accurate, but traditional verification metrics strongly penalise displacement errors, which high resolution models by nature are more prone to (e.g. Mass et al 2002). Human forecasters (e.g. Roebber et. al. 2004) and/or the use of model ensembles (e.g. Peralta et. al., 2012) or other post-processing techniques (e.g. Theis et. al., 2005)) are needed to account for uncertainty in this high resolution model output, and appropriately convey risk to end users.
To provide more useful automated quantitative ashfall forecasts from a HYSPLIT/WRF system that account for uncertainty in the NWP winds and eruption parameters, we could follow the example of high resolution NWP and use an ensemble of model runs based on multiple NWP forecasts and a range of eruption parameters.
For airborne ash the Wellington VAAC does this to some extent by running a small HYSPLIT ensemble, with a range of eruption parameters, and with meteorological data from 3 NWP models. Dare et al., (2016) examined the impact of atmospheric uncertainty with a 24 member NWP model ensemble, again for airborne ash. Large ensemble systems are not yet used operationally by VAACs (WMO 2012, 2015). We believe similar ensemble based approaches that also include eruption source uncertainty are needed for ash fall forecasts.
An immediately achievable way of including uncertainty into HYSPLIT predictions would be to follow the Wellington VAAC approach and make the predictions based on multiple NWP models for each hypothetical eruption. Further investigations would be required to determine how best to present this output; options include the most conservative approach of outputting the union of ensemble ash fall areas, the contour of a specific percentile of ash depth (e.g. Draxler et al 2003), or the probability of exceedance for a specific ash depth.
By moving to the HYSPLIT/WRF we have eliminated the gross forecast errors that ASHFALL will produce in a complex wind field. The approach that the existing ASHFALL model takes to address meteorological uncertainty (an artificially large diffusion coefficient) apportions too much of this uncertainty close to the vent, and even upwind, whereas NWP wind errors should grow downwind from the vent.
It should also be noted that as well as the uncertainties of the wind pattern for ash forecasting, there will be large uncertainties in the eruption parameters. We cannot predict what eruption (i.e. magnitude, plume height) will next take place from any particular volcano, and when an eruption starts we often have very limited information.
We have successfully set up the use of HYSPLIT to give forecasts of volcanic ash deposition, were a New Zealand volcano to erupt. These forecasts use a much more detailed atmospheric model than the forecasts produced by ASHFALL, in particular the wind pattern varies in 3 spatial dimensions, rather than one. This gives potentially more accurate forecasts, particularly in situations with complex wind patterns.
Comparison of HYSPLIT hindcasts of the ash deposition from the 8 August 2012 Te Maari eruption from Mt Tongariro showed that HYSPLIT would have accurately forecast the narrow ash plume observed about 12 km downwind of the vent, but there was apparently a discrepancy between the forecast and actual wind direction further downwind, that significantly altered where ash was deposited. This emphasizes that we need to give an indication of what areas are at risk of volcanic ash, rather than just giving a single best estimate of the ash distribution.
The work leading to this paper was funded from GNS Science Core Funding, and MetService Internal Funding.
TH provided all ASHFALL simulation output and performed the comparison of both models with deposition observations for the Te Maari case. CD provided all HYSPLIT output. Both authors drafted the manuscript. Both authors read and approved the final manuscript.
The authors declare that they have no competing interests.
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- Bonadonna C, Ernst GGJ, Sparks RSJ. Thickness variations and volume estimates of tephra fall deposits: the importance of particle Reynolds number. J Volcanol Geotherm Res. 1998;81:173–87.View ArticleGoogle Scholar
- Carey S, Sigurdsson H. Influence of particle aggregation on deposition of distal tephra from the May 18, 1980, eruption of Mount St. Helens volcano. J Geophys Res. 1982;87(B8):7061–72.View ArticleGoogle Scholar
- Crawford A, Stunder B, Ngan F, Pavolonis MJ. Initializing HYSPLIT with satellite observations of volcanic ash: A case study of the 2008 Kasatochi eruption. J Geophys Res Atmos. 2016;121:10786–803. doi:10.1002/2016JD024779.
- Crouch JF, Pardo N, Miller CA. Dual polarisation C-band weather radar imagery of the 6 August 2012 Te Maari eruption, Mount Tongariro, New Zealand. J Volcanol Geotherm Res. 2014;286:415–36. doi:10.1016/j.jvolgeores.2014.05.003.View ArticleGoogle Scholar
- Dare RA. Sedimentation of volcanic ash in the HYSPLIT dispersion model. CAWCR Technical Report No. 079. Melbourne: Centre for Australian Weather and Climate Research; 2015.Google Scholar
- Dare RA, Smith DH, Naughton MJ (2016) Ensemble Prediction of the Dispersion of Volcanic Ash from the 13 February 2014 Eruption of Kelut, Indonesia. J Appl Meteor Climatol doi: http://dx.doi.org/10.1175/JAMC-D-15-0079.1.
- Draxler RR. Evaluation of an ensemble dispersion calculation. J Appl Meteor. 2003;42:308–17.View ArticleGoogle Scholar
- Draxler RR, Hess GD. DESCRIPTION OF THE HYSPLIT_4 MODELING SYSTEM, NOAA Technical Memorandum ERL ARL-224. 2010 revision. Silver Spring: NOAA Air Resources Laboratory; 1997.Google Scholar
- Ganser GH. A rational approach to drag prediction of spherical and nonspherical particles. Powder Technol. 1993;77:143–52.View ArticleGoogle Scholar
- Heffter JL, Stunder BJB. Volcanic Ash Forecast Transport And Dispersion (VAFTAD) model. Wea Forecasting. 1993;8:533–41.View ArticleGoogle Scholar
- Hurst AW. ASHFALL - a computer program for estimating volcanic ash fallout : report and users guide. Wellington: Institute of Geological & Nuclear Sciences. Institute of Geological & Nuclear Sciences science report 94/23; 1994. p. 22.Google Scholar
- Hurst AW, Smith WD. Volcanic ashfall in New Zealand : probabilistic hazard modelling for multiple sources. N Z J Geol Geophys. 2010;53:1–14.View ArticleGoogle Scholar
- Hurst AW, Turner R. Performance of the program ASHFALL for forecasting ashfall during the 1995 and 1996 eruptions of Ruapehu volcano. N Z J Geol Geophys. 1999;42:615–22.View ArticleGoogle Scholar
- Hurst AW, Jolly AD, Sherburn S. Precursory characteristics of the seismicity before the 6 August 2012 eruption of Tongariro volcano, North Island, New Zealand. J Volcanol Geotherm Res. 2014;286:294–302. doi:10.1016/j.jvolgeores.2014.03.004.View ArticleGoogle Scholar
- Jones A. Atmospheric dispersion modelling at the Met Office. Weather. 2004;59:311–6.View ArticleGoogle Scholar
- Kantha LH, Clayson CA. Small Scale Processes in Geophysical Fluid Flows, vol. 67. San Diego: International Geophysics Series, Academic Press; 2000. p. 883.View ArticleGoogle Scholar
- Lube G, Breard ECP, Cronin SJ, Procter JN, Brenna M, Moebis A, Pardo N, Stewart RB, Jolly A, Fournier N. Dynamics of surges generated by hydrothermal blasts during the 6 August 2012 Te Maari eruption, Mt. Tongariro, New Zealand. J Volcanol Geotherm Res. 2014;286:348–66. doi:10.1016/j.jvolgeores.2014.05.010.View ArticleGoogle Scholar
- Macedonio G, Pareschi MT, Santacroce R. A numerical simulation of the plinian fall phase of 79 A.D. eruption of Vesuvius. J Geophys Res. 1988;93(B12):14817–27.View ArticleGoogle Scholar
- Mass C, Ovens D, Westrick K, Colle B. Does Increasing Horizontal Resolution Produce More Skillful Forecasts? Bull Amer Meteor Soc. 2002;83:407–30.View ArticleGoogle Scholar
- Mastin LG, Van Eaton AR, Durant AJ. Adjusting particle-size distributions to account for aggregation in tephra-deposit model forecasts. Atmos Chem Phys. 2016;16:9399–420. doi:10.5194/acp-16-9399-2016.View ArticleGoogle Scholar
- Pardo N, Cronin SJ, Nemeth K, Brenna M, Schipper CI, Breard E, White JDL, Procter J, Stewart B, Agustin-Flores J, Moebis A, Zernack A, Kereszturi G, Lube G, Auer A, Neall V, Wallace C. Perils in distinguishing phreatic from phreatomagmatic ash : insights into the eruption mechanisms of the 6 August 2012 Mt. Tongariro eruption, New Zealand. J Volcanol Geotherm Res. 2014;286:397–414. doi:10.1016/j.jvolgeores.2014.05.001.View ArticleGoogle Scholar
- Peralta C, Ben Bouallègue Z, Theis SE, Gebhardt C, Buchhold M. Accounting for initial condition uncertainties in COSMO-DE-EPS. J Geophys Res. 2012;117:D07108. doi:10.1029/2011JD016581.View ArticleGoogle Scholar
- Pfeiffer T, Costa A, Macedonio G. A model for the numericalsimulation of tephra fall deposits. J Volcanol Geotherm Res. 2005;140:273–94. doi:10.1016/j.jvolgeores.2004.09.001.View ArticleGoogle Scholar
- Roebber P, Schultz D, Colle B, Stensrud D. Toward Improved Prediction: High-Resolution and Ensemble Modeling Systems in Operations. Wea Forecasting. 2004;19:936–49.View ArticleGoogle Scholar
- Rose WI. Comment on `Another look at the calculation of fallout tephra volumes’ by Judy Fierstein and Manuel Nathenson. Bull Volcanol. 1993;55:372–4.View ArticleGoogle Scholar
- Scott BJ, Potter SH. Aspects of historical eruptive activity and volcanic unrest at Mt. Tongariro, New Zealand : 1846–2013. J Volcanol Geotherm Res. 2014;286:263–76. doi:10.1016/j.jvolgeores.2014.04.003.View ArticleGoogle Scholar
- Self S, Sparks RSJ, Booth B, Walker GPL. The 1973 Heimaey Strombolian Scoria deposit, Iceland. Geol Mag. 1974;111:539–48.View ArticleGoogle Scholar
- Stein AF, Draxler RR, Rolph GD, Stunder BJB, Cohen MD, Ngan F. NOAA's HYSPLIT atmospheric transport and dispersion modeling system. Bull Amer Meteor Soc. 2015;96:2059–77. doi:10.1175/BAMS-D-14-00110.1.View ArticleGoogle Scholar
- Suzuki T. A theoretical model for distribution of tephra. In: Shimozuru D, Yokohama I, editors. Arc volcanism: physics and tectonics. Tokyo: Terra Scientific Publishing; 1983. p. 95–113.Google Scholar
- Theis SE, Hense A, Damrath U. Probabilistic precipitation forecasts from a deterministic model: a pragmatic approach. Met Apps. 2005;12:257–68. doi:10.1017/S1350482705001763.View ArticleGoogle Scholar
- Turner R, Moore S, Pardo N, Kereszturi G, Uddstrom M, Hurst AW, Cronin S. The use of Numerical Weather Prediction and a Lagrangian transport (NAME-III) and dispersion (ASHFALL) models to explain patterns of observed ash deposition and dispersion following the August 2012 Te Maari, New Zealand eruption. J Volcanol Geotherm Res. 2014;286:437–51. doi:10.1016/j.jvolgeores.2014.05.017.View ArticleGoogle Scholar
- Walker GPL. The Waimiha and Hatepe plinian deposits from the rhyolitic Taupo Volcanic Centre. N Z J Geol Geophys. 1981;24:305–24.Google Scholar
- World Meteorological Organization. VAAC “Inputs and Outputs” (Ins and Outs) Dispersion Modelling Workshop: Final Report. Washington DC; 2012.Google Scholar
- World Meteorological Organization. 7th International Workshop on Volcanic Ash, Workshop report. Alaska; 2015.Google Scholar