Major primary faults in Sweden are for example: the Pärve Fault [7] and Lansjärv Fault [8] in northernmost Sweden, the Hornslandet Fault [4]) in central Sweden, the Mälardalen E-W Fault [4] [9] [10], the Lake Vättern Fault [11] [12] and the Mid-Kattegatt Fault [4] [13].

Besides the main fault deformations, secondary faults and fractures were generated, too. There are examples of quite significant secondary bedrock deformations in Sweden [4] [10] [14] [15].

Bedrock cave deformation is a quite specific type of deformation [15] [16]. Most of them must have a seismotectonic origin [15] [17]. Some of them, however, are caused by methane-venting-tectonics; i.e. they are the function of explosive venting when methane ice is suddenly transformed into methane gas [4] [5] [10] [14].

Massive bedrock avalanches are initiated by earthquake shaking and bedrock fracturing, but driven by gravity. There are quite clear examples of this in Sweden [4] [15] [16] [17].

The main processes of sediment deformations are directly linked to the ground shaking as further discussed below (Section 4). Methane venting is an additional process [4]. Earth slides, initiated by earthquake shaking or methane venting are, of cause, driven by gravity. The Storegga submarine slide outside the Norwegian coast is of enormous dimensions (e.g. [18]), and it is linked to methane venting (e.g. [19]).

There are numerous different processes that may generate sediment deformation, such as: bioturbation, erosion/re-deposition, load-casts, slides and turbidites, sediment adjustments, liquefaction, tsunamis, glacial-tectonics, ice-rafting, and peri-glacial activities (on land). In this paper, I will limit the discussion to deformations of seismic origin, i.e. seismites, recorded in Sweden (cf. [4] [20]).

Everything moved out of primary, in situ, position due to earthquake shaking may be called a “seismite” [20]. Consequently, this includes dislocated rock fragments, rock avalanches, seismotectonic caves, earth slides, liquefaction, tsunamites and turbidites, as illustrated in Figure 2. As to particle size, this implies a range from blocks to clay. Via magnetic methods, we may even record fluidized reorganization of very fine particles in the interstitial water [21].

Sweden is full of excellent liquefaction structures [4] [22] [23] [24] [25]. Before our studies on paleoseismology at the P & G-unit of Stockholm University, it was not understood that Sweden had suffered both frequent and high-magnitude earthquake events in the past [11] [26]. Therefore, the structures could not be correctly interpreted. Descriptions to local Quaternary maps of Sweden often show photos of deformed sediments labelled “water escape structures”. Now, we know that these pictures record quite clear liquefaction structures ([4] e.g. the remarkable site of Olivelund, pp. 234-236). In another case, quite typical liquefaction structures ([4] the Hunnestad site, pp. 281-282, later more fully described in [13]) were even termed “an ice wedge”. We therefore had to start, so to say, from the beginning, and there is a general lack of comparative studies in Sweden (except for [27] and [28]).

The phenomenon of “liquefaction” refers to the process where a sediment layer or a part of a sediment layer is transformed into a fluid or fluidized stage (from Latin: liquid facere). This occurs post-depositionally (sometimes also “syn-sedimentary”). There are different ways of generating liquefaction. The most common process is earthquake shaking [25].

The shaking motions at an earthquake may lead to a reorganisation of the internal distribution of grains and water so that the sediment becomes fluid. This makes deposits of sand and course silt most susceptible for liquefaction. Also, fine gravel may fairly easily become liquefied. Liquefaction of courser and finer sediments (course gravel to pebbles and fine silt to clay) only occurs rarely and under special conditions. The post-depositional liquefaction of a stratified sandy bed implies that the original stratification becomes totally or partly erased into a structureless bed (Figure 3). By magnetic methods, we have shown that also clay and fine silt beds may be subjected to an internal fluidization [21].

A liquefied bed will behave like a “heavy fluid” allowing big blocks and eroded fragments to “swim” in the liquefied bed (Figure 4). This also opens for density redistribution heavy beds sinking down and lighter beds flaming upwards (Figure 5). This also leads to venting of liquefied material and formation of mud-volcanoes. The size of venting structures and the material to become vented are strongly linked to the magnitude of earthquake.

Liquefaction may strike a stratified sedimentary bed quite differently; strongly deforming some beds and leaving others virtually unaffected (Figure 6). The material vented or liquefied behaves quite differently with respect to grain sizes. Whilst the material forming the vented or liquefied structure is primarily flow-oriented, the micro-particles may be randomly or magnetically re-oriented as further discusses under crypto-deformations.

Also laterally, the liquefaction strikes sedimentary beds quite differentially. So, for example, did we record only vaguely deformed varves in a shallow trench, but totally mess of heavily liquefied deposits in a 2 m deep trench only 20 m away ([21] site: Mehedeby).

Because earthquakes usually are not single events, but rather a cluster of shocks and after-shocks, one would expect to see not just one phase of liquefaction, but multiple phases [4]. Therefore, it seems significant that we, at several events, were able to record multiple phases of liquefaction. At the 9663 BP paleoseismic event, we recorded five successive phases (Figure 7) in two sites located 35 km apart, and interpreted those phases in terms of shock and after-shocks.

The size and type of liquefaction structures have a bearing on the magnitude. In some cases we have recorded the venting of gravel, even course gravel and pebbles (Figure 8). This calls for magnitudes in the order of M > 8. One such event is dated at 10,388 vBP and another at 6100 BP [4] [9] [24] [25].

The spatial distribution of a liquefaction event is more or less linearly related to the magnitude of the earthquake (Figure 9). Liquefaction events are recorded at numerous sites in Sweden [4] [9] [24] [25].The spatial distribution of one and the same liquefaction event gives evidence of high-magnitude paleoseismic events. The paleoseismic event occurring in the autumn of varve 10,430 BP generated liquefaction over an area of 320 × 100 km, and the event in varve 9663 BP over an area of at least 80 × 40 km, which can be used to estimate the corresponding magnitudes according to Figure 9. It is the time resolution as to a single varve (even season of a varve) that allow us to reconstruct the past spatial distribution of liquefactions, and by that of obtaining a magnitude estimate [4] [10].

Even the frequency of paleoseismic varves was unusually high. So for example, 7 events were recorded with 102 years ranging from varve 10,490 to 10,388 BP [9] [10].

Liquefaction events are also recorded in Late Holocene deposits. An event causing strong liquefaction is dated 4800 BP [4] [6] [10], and a younger event of about 2800 BP generated liquefaction at sites 52 km apart [29].

The seismic wave passing over a site generates an expansion/contraction pumping effect, recorded both in bedrock and in sediment deformations [4]. At two sites in [4] (viz. at Hög, pp. 122-132, and at Olivelund, pp. 234-236), we recorded a wavy pattern in the top of the deformed and liquefied sedimentary sequence; in Hög the wavelength was in the order of 2 - 3 m and in Olivelund of about 50 m (Figure 10).

Seismic shaking may also generate wavy patterns of previously horizontal sand and clay beds (Figure 11; cf. [4] and [21]). The combination of liquefaction fluidization and ground shaking also generated the sinking down of pebbles and stones in the liquefied beds of sand below as shown in Figure 12.

When sediments become liquefied and the fluid masses move and vent, covering sediments have to accommodate for the space changes. This gives rise to additional deformations and micro-faulting of sedimentary units dislocated as illustrated in Figure 13.

Extensive turbidites are often formed by the sediment masses set in motion by slides, liquefaction and tsunami waves (Figure 2). They stick out as distinct “marker-varves” (Figure 14). This allows a very precise dating with respect to the Swedish Varve Chronology (e.g. [30]).

The clay deposited in the Baltic basin in front of the receding ice margin became annually stratified in grains-size, colour and geochemical content. By counting the varves, De Geer [31] was able to build up a chronology for the last 10,000 - 12,000 years, known as The Swedish Timescale. After intensive additional work and revisions by numerous scientists, the time-scale now covers about 14,000 years (e.g. [30]).

The turbidites of the paleoseismic event of 10,430 and 9663 varves BP are both varve specific and provides direct dates. Out of the 62 paleoseismic events included in the Second Paleoseismic Catalogue of Sweden [5], 31 events are dated by varves.

In the Stockholm area, 4 subsequent paleoseismic events were recorded and due to their deformations of varves dated at 10,490, 10,469, 10,447 and 10,430 varves BP ([4] p. 229-232), implying a recurrence time of about 20 years. Including the more westerly parts of the E-W fault passing the Lake Mälaren area, the sequence of paleoseismic events was later updated at 7 events within 102 years (see Figure 10 in [10]).

The 10,430 varve BP event is special, because in this case we can assign a seasonal resolution to the autumn of this varve [4] [9] [10] [20] [32]. In 3 sites over a distance of 76 km, the earthquake event is pinpointed to the autumn of the varve 10,430. This is illustrated in Figure 15 (to be compared with the actual sedimentary columns in Figure 6 of [20]). Section A1 shows a concordant stratigraphy with a change from freshwater to brackish water varves at the varves 10,431/10,430 transition, which corresponds to a major tsunami event opening a free connection to the Atlantic [4] [34]. Section A2 shows an erosional depression, which began to be filled by the autumn unit of varve 10,430 (indicating the return to normal sedimentary conditions after the paleoseismic event and tsunami event). Section B (Lake Albysjön) shows a slump injected into the autumn unit of varve 10,430. Section C (Lake Dammsjön) shows a strongly irregular and flamelike autumn unit of varve 10,430 (the summer and winter units remaining homogeneous).

The first record of a tsunami event was found in 1995. This event was linked to the 10,430 varves BP paleoseismic event. It was followed by the discovery of a tsunami event linked to the 9663 varves BP event. After preliminary reports [33] [35] [36], the full report followed [4], [33] and [36]. The relation between tsunami wave height and earthquake magnitude is given in [37]. A general account of tsunami deposits is given in [38].

Up to now, a total of 19 events have been documented and described in Sweden (Table 1). They are traced both in on-shore environment as intra-clay sand-layers containing a planctonic microfossil fauna and flora, and in offshore environment as extensive turbidites (below). In all cases, the tsunami events can be linked to other records of paleoseismic events, such as liquefaction and bedrock deformation [4] [33] [36].

At the 9663 varves BP paleoseismic event, we have traced the ingression of a tsunami wave in 14 separate lakes spanning an area of 175 × 25 km. The wave height must have been, at least, 15 m. The tsunami deposits consist of sandy layers of graded bedding (fining upwards) within clay beds, implying an interruption in the normal depositional conditions. The microfossil content is planktonic indicating an open sea or lake origin. Sometimes, we see a sequence of multiple graded bedding units from a train of tsunami waves.

The 10,430 BP paleoseismic event set up a very strong tsunami, washing the Närke Straight free of pack-ice so that the entire Baltic basin turned brackish within 1 single year [4] [33] [36]. The wave height must have been in the order of 15 - 20 m. The event is recorded in 9 sites covering an area or 320 × 200 km.

At about 2900 BP, a major tsunami wave was set up by an explosive sudden venting of methane gas [4] [6] [33] [36], and at around 900 BP an about M 7 paleoseismic event set up a tsunami that covered two Viking-ships with a thick silt bed [36].

Figure 16 gives an instructive example of the interaction between paleoseismic liquefaction and a tsunami event. The ice receded in the varve 9747 BP, 84 annual varves were deposited, and then the 9663 BP paleoseismic event occurred causing both liquefaction and a tsunami. The sandy deposits of the events in question are covered by micro-varves and Baltic clay (and finally a cap of littoral sand from the emergence).

The basal silt became liquefied by the 9663 BP paleoseismic event, vented through clay bed (also sending injections horizontally in-between some of the varve units), and mushroomed at the seabed, where it interacted with a tsunami wave. We cleaned the lower clay surface in Pit 4, and exposed furrows and wave patterns indicating that the tsunami came from the open sea to the east (i.e. from the right to the left in Figure 16). Subsequent studies confirmed that the epicentre was located to the east along the Hornslandet Fault [4].

Major turbidites occur in varves 10,430, 9663 and 9428 BP. Originally, they were all interpreted in terms of so-called “drainage varves” [32]. Because of their direct association with major paleoseismic events, we can now be sure that they all are turbidites generated by strong paleoseismic events [4] [20] as illustrated in Figure 2. Hence, they are seismites (Figure 12).

These turbidites have been recorded in numerous cores and section over wide areas; 300 × 200 km for the 10,430 BP event and 320 × 90 km for the 9663 BP event. The mode of deposition seems to be a combination of gravity driven density flow along the bottom (Figure 2) and seabed trimming by tsunami waves according to the model proposed by [33] [36] as shown in Figure 17.

By magnetic methods, it has been possible to detect internal “crypto-deformations” not visible in structural deformations [21] and [39]. I will here give four different cases from Sweden.

A folded structure may originate from a plastic deformation due to glacial-tectonics or slide movements. It may also be generated by liquefaction. In the case of a plastic fold, the turned over part should have a reversed inclination. In the late 90s, I noted that a fold in association with a paleoseismic event in south-central Sweden had normal inclination also in the over-turned part (Figure 18). I took this as evidence that the fold was a liquefaction structure formed under so fluidized conditions that the magnetic grains were able to move freely and could be re-oriented with respect to the magnetic forces. This provided a new method of discriminating between plastic and fluid folds [21].

In a sequence of 34 concordant varves preceding the 10,430 BP paleoseismic event, we recorded a 90˚ eastward rotation of the ChRM values in the lower 20 varves. This must imply that the ChRM carrying grains were moved by the earthquake shaking in a rotational manner increasing upwards by 90˚, the AMS carrying grains being aligned with the main depositional flow direction and the varves being virtually un-deformed.

In a major venting mushroom structure of the 9428 BP paleoseismic event, we observed an inward-upward-outward flow of the sandy-silty mushroom structure itself, a totally random distribution of the AMS grains and a perfectly geomagnetic field orientation of the ChRM carrying very fine particles of the interstitial water. Consequently, the earthquake shaking generated a laminar flow of the mushroom itself, a turbulent flow of the AMS particles, and a free flow of the very fine ChRM carrying particles.

Finally, we noted that the earthquake shaking and free liquid motion of ChRM particles implied a second chance of alignment with respect to the geomagnetic field. Therefore, we noted a spike of increased paleomagnetic intensity, decreasing laterally from the epicentre. We termed this additional magnetization: “seismomagnetization”. At the paleoseismic event 10,430 BP, such an intensity peak (“The Gålö Intensity Peak”) is recorded over an area of 500 × 600 km. This is a remarkably large area, and can only be understood in terms of a very strong earthquake event: M >> 8 [4] [10].

When we see no visible sedimentary deformation and the AMS and/or ChRM grains are deformed, we may speak of “crypto-deformations” [21].