Three other signals of likely seismic origin occurred on 14 March, 10 April, and 11 April 2019. These signals are more ambiguous to the InSight team than the one on 6 April, but do not appear to be clearly associated with atmospheric disturbances or other known noise sources. They are smaller than the event on 6 April and were only detected by the more sensitive broadband sensors. The team will continue to study these events to try to determine their origin.

Based on these first records, marsquakes seem to be distinct to earthquakes. According to their size and long duration, they are more similar to quakes recorded on the Moon by the Apollo programme. Whereas on Earth plate tectonics is the dominant process that provokes quakes, on the Moon the cooling and contraction causes tremors. The relevant processes at Mars are not yet fully understood. In any case, stress is built up over time until it is strong enough to break the crust. Different materials can change the speed of seismic waves or reflect them, allowing scientists to use these waves to learn about the interior of a planet and model its formation. The events recorded until now are too small to provide useful data on the deep Martian interior. Nevertheless, they mark a milestone of the InSight mission, proving the efficiency of the data processing and analysis capabilities, both developed at ETH Zurich.

Despite the very large number of deep boreholes drilled worldwide, data on earthquakes occurring in connection with them are rather sparse. One reason for this is that the probability of such quakes is very low. Another is that many deep boreholes have been drilled in uninhabited areas, so potentially noticeable quakes may not have been felt and reported by the public. In many places, such boreholes have not been - and are still not being - seismically monitored. Consequently, it is impossible to reliably record smaller induced earthquakes. In Switzerland, for example, a number of microquakes were recorded when the borehole for the Basel geothermal energy project was cemented. The strongest of these had a magnitude of 0.7, meaning that it released 500 times less energy than a magnitude 2.5 quake. Earthquakes above this magnitude can usually be felt.

The physical processes behind earthquakes triggered in certain circumstances by drilling boreholes are well understood. Deep boreholes sometimes alter local stresses and pore pressures in rock, and in some cases this can reactivate a nearby tectonically pre-stressed fracture, causing an earthquake. However, such stress changes usually only occur in the following two situations: firstly, when drilling into a stratum with high fluid pressures. In this case, under certain conditions, the rock fluid (liquid or gas) can find its way into the borehole, causing overpressure that can usually be reduced in a controlled manner. Alternatively, the borehole is sealed at the corresponding place deep underground. Secondly, when boring into a very liquid-permeable stratum or rock of very low strength. If this happens, some of the drilling fluid or cement may enter the surrounding rock. The drilling fluid is needed to bring the drilling dust to the surface and stabilise the borehole during the driving process. Once a section has been drilled, the borehole is lined with cemented pipe to keep it open in the long term. In most cases, though, stress changes only affect small rock volumes. So the probability of activating quite a large, pre-stressed fracture and thus triggering a fairly large, potentially noticeable earthquake is extremely low.

The Swiss Seismological Service (SED) at ETH Zurich does not normally recommend seismic monitoring in its Guide for Managing Induced Seismicity for deep boreholes (e.g. exploratory drilling). Nonetheless, to record evidence and clarify the distinction between natural and induced seismicity, it may make sense to install an additional monitoring station near a drill site. For this very purpose, to cite just one example, the SED is currently consolidating its network on behalf of Switzerland's National Cooperative for the Disposal of Radioactive Waste (Nagra) with a view to monitoring exploratory drilling in northeastern Switzerland.

The two strongest earthquakes felt over the largest areas by the Swiss population occurred on 17 January and 1 February 2018 in Austria's Kloster Valley (Montafon) near the Swiss border. Both quakes reached a magnitude of 4.1. The most powerful earthquake in Switzerland itself, with a magnitude of 3.2, occurred on 23 August near the twin-peaked mountain Dents de Morcles in the Canton of Valais. The SED received around 400 reports from people who felt this quake, mainly in the Rhone Valley, whose soft subsurface particularly intensified the shaking. Other earthquakes, some of which were also clearly felt, occurred on 15 and 16 May near Châtel-St-Denis in the Canton of Fribourg (with magnitudes of 3.1 and 2.9), on 3 November near Martigny in the Canton of Valais (magnitude 2.9) and on 29 December near Fribourg (magnitude 2.9). Only the quakes in the Kloster Valley ended up causing minor damage, such as cracks in buildings' façades.

In addition, last year saw the occurrence of some remarkable earthquake swarms. A swarm entails numerous quakes occurring over a fairly long period, without there being any clear sequence of foreshocks, mainshock and aftershocks. The most notable swarm involved a series of earthquakes northeast of St. Léonard, near Sion in the Canton of Valais. This sequence was related to a fault that has repeatedly been associated with phases of heightened seismic activity since 2014. It is believed to be part of the Rhone-Simplon fault, which appears to be broken into separate segments in this area. Another earthquake sequence worth mentioning occurred in the border area between Italy, France and Switzerland, in the east of the Mont Blanc Massif. Last year, the SED pinpointed the locations of close to 100 earthquakes with magnitudes between 0 and 2.2 in that area.

In general, in 2018, as in previous years, most earthquake activity occurred in the Valais region, the Canton of Graubünden and the areas along the Alpine front. Despite this concentration of seismic activity, historically it has been shown that no parts of Switzerland are earthquake-free regions. Based on the long-term average, a serious earthquake with a magnitude of 6 or more occurs in the earthquake country Switzerland every 50 to 150 years.

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