Table 3 Input values for the FLOWGO (e.g., Mossoux et al. 2016; Chevrel et al. 2018) modelling
From: Thermal impacts of basaltic lava flows to buried infrastructure: workflow to determine the hazard
Parameter | Value | Source/Justification |
|---|---|---|
Down-flow increment | 10 m | |
Slope | Varies between 1.4 to 1.9° | Local topography |
Channel width | Varies between 26 and 54 m | MOLASSES modelling |
Channel depth | Varies between 17.5 and 19.2 m | MOLASSES modelling |
Viscosity | 1000 Pa s | default |
Emissivity | 0.95 | Patrick et al. (2004) |
Thermal conductivity | 4.85 W/m°C | Tsang et al. (2019b) |
Basal temperature | 891 °C | Tsang et al. (2019b) |
Core to base distance | 20% | Nowak (1995) |
Eruptive temperature | 1200 °C | Kereszturi et al. (2014a) |
Crustal temperature | 827 °C | Tsang et al. (2019b) |
Buffer | 140 °C | Default |
Crustal cover | 0.6 | Default |
Crust to velocity relationship | −0.00756 | Default |
DRE density | 2650 kg/m3 | Kereszturi et al. (2014a) |
Vesicularity | 0.15 | Kereszturi et al. (2014a) |
Bulk density | 2490 kg/m3 | Kereszturi et al. (2014a) |
Wind speed | 5.1 m/s | Hayes et al. (2018) |
Ch | 0.0036 | Default |
Air temperature | 15.9 °C | CliFlo (2019) |
Air density | 1.22 kg/m3 | |
Air specific heat | 1006 | |
Phenocryst content | 0.15 | Kereszturi et al. (2012) |
Crystals grown during cooling | 0.9 | |
Cooling range | 300 °C | Default |
Latent heat of crystallisation | 3.5 × 105 | Default |
r | 1.51 | Default |