2.1 Tectonic geomorphology of the Ulakhan fault across the Buyunda fan

The Buyunda alluvial fan builds two distinct lobes where it enters the Seymchan Basin at its southeastern end (Figs. 2 and 3). The inner lobe surface is steeper and preserves a dense network of braided-fan distributary systems, some of which may have been active until recently. The outer lobe has gentler gradients and is fed today by input from several smaller fans along its southern edge (Fig. 2). The lobes together occupy ∼20 % of the modern-day basin floor: the inner lobe measures ∼190 000 km², the outer lobe (including the inner lobe) ∼480 000 km². The fan is asymmetric and has a long axis oriented towards the northwest (Fig. 2).

The Buyunda river, which enters the basin through a narrow north-trending gorge, flows along the eastern side of the alluvial fan and bypasses its earlier apex. The Buyunda river forms a braided channel, ∼1 km wide, which trends almost linearly northeast, parallel to the fan edge, before looping around an isolated remnant of the Jurassic basin floor and turning northwest, along the northern basin margin. A second braided channel system, which from its sharp definition in satellite imagery (Fig. 3c) seems very recently abandoned, runs almost exactly parallel to the present-day system, on its western side, at 2–5 km distance. This earlier course of the river flowed to the west of the Jurassic remnant. Several similar braided channel systems, representing earlier generations of the Buyunda river, occur across the fan surface but become progressively more difficult to distinguish from one another in a westerly direction (Fig. 2).

In 2012, we visited the western edge of the fan where it intercepts the fault, which is marked by a lake (Lake Rovnoye) (Figs. 3, 4, 5), approximately 1 km long and roughly triangular in shape. Immediately east of it, there is a pronounced 3–5 m high scarp, trending in a roughly ESE direction (105^∘). Adjacent to the scarp to its north are a series of 10–50 m wide basins (Fig. 4). We were able to follow these basins and the scarp for ∼1.2 km to the ESE, before a noticeable break at the point where a second small lake is found, also visible on aerial imagery, where there are three right-stepping en échelon scarps for a distance of ∼900 m (Figs. 3 and 4). These have variable orientations, with the two, more southerly lying scarps trending close to E–W, whilst the isolated segment of the main scarp further north trends ∼125^∘. There is also another small lake and basin at the tip of the most southerly of the three scarps in this region. At this point, the scarps merge again and continue as a single line. The scarps bound a wider (up to 500 m) uplifted portion of the fan to the south, also visible from DEM data.

Figure 4(a) Un-interpreted aerial photo picture of ridge and scarp, showing sample localities (red stars) and names. Outline of Fig. 5 indicated. (b) Interpreted image showing ridge area south of scarp (dark shaded), fossil channel system (light blue outline) and offset channel bank feature (light blue solid shading). Also shown are linear velocity vectors based on Okh–NAm poles of Sella et al. (2002) and Seno et al. (1996).

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The basins along the scarp showed signs of intermittent flooding and transport of some alluvial material, including occasional deposits of pebbles up to 5 cm diameter. Field reconnaissance, aerial photographs and satellite imagery suggest that present-day drainage runs west-northwest into Lake Rovnoye, and parallel to the scarp (Figs. 3, 5).

Figure 5(a) Magnification of aerial photo showing interpreted, northwest-oriented palaeodrainage and sample localities ul1 and ul2, interpreted to be offset as part of abandoned channel system. (b) Aerial photo with interpretation, showing offset palaeo-channel feature. (c) Landsat (567 band) detail, showing hydrology of scarp and ridge with a dry ridge (dark coloured area) bounded north and south by saturated zone (light coloured area). For explanation of hydrology, see text.

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In 2011, we visited a region immediately ESE of the 2012 campaign, starting from the point where the main road on the Buyunda fan intersects the apparent trace of the fault. Here, we encountered a series of ∼100–200 m long, 10–20 m wide depressions, almost symmetric in profile, with a total relief of 5–8 m from the deepest point (Fig. 6). These basins follow a fairly continuous 110–120^∘ trend to the point where they intersect with the 2012 field area.

Figure 6Field photographs and interpretations of the main fault scarp near Lake Rovnoye (a) and a depression with a smaller scarp further east (c). An aerial photograph (b) shows approximate locations of the views and view orientations.

The aerial photographs and DEM show the wider fluvial and tectonic geomorphology of the Buyunda fan in the vicinity of the scarp (Figs. 3, 4). The pronounced scarp across the Buyunda fan, visited in 2012, can be traced over a distance of ∼3.5 km, starting immediately to the east of Lake Rovnoye. The scarp shows a consistent 1.5–5 m relief (southern side higher), as can be seen by both fault-normal topographic profiles and relief maps from the DEM (Fig. 7). It terminates into the series of narrow, elongated depressions encountered in 2011, which form a linear trend oriented 115^∘, and extend for a further 2.5 km eastwards. There are approximately 10 of these depressions, with smaller vertical offsets than on the scarp, further west. Still further eastwards, the series of smaller depressions give way to three much larger (∼500 m ×100–200 m wide and 10 m deep) basins, aligned in the same 115^∘ orientation and spread over a distance of ∼2.5 km. These may be dried-out thermokarst lakes (e.g. Bouchard et al., 2016). These also coincide with the apparently more recently active part of the fan surface, judging by the still fresh appearance of the preserved braided channel systems in satellite imagery. Similar depressions also occur in other places off-trend of the scarp.

Figure 7Topographic profiles, showing vertical offsets across the scarp on the Buyunda fan. Offsets are close to maximum near Lake Rovnoye (profiles 1 and 2) but diminish eastwards over a distance of ∼5 km. From Lake Rovnoye westwards there is also no vertical offset. Dashed lines are estimated average elevation of surface either side of fault for determining vertical offset.

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The linear features we have identified are aligned close to parallel to various predicted Okh–NAm linear velocity vectors (Sella et al., 2002; Seno et al., 1996; Apel et al., 2006). There is an especially close match to the present-day GPS-based REVEL global Euler vector (Sella et al., 2002), with magnitude ∼6 mm yr⁻¹. The best-fitting Euler vector based on spreading rates and earthquake focal mechanisms, and hence considered a longer-term estimate (up to 3.5 Myr) (Seno et al., 1996), is slightly more oblique to the trend and of lower magnitude (∼4 mm yr⁻¹) (Fig. 4).

We can thus trace a linear feature across the inner fan surface made up from west to east of a distinct fault scarp, a series of narrow elongated depressions, and a series of possible dry, thermokarst lakes over a total distance of ∼10 km. The linear trend terminates in the modern-day Buyunda river channel. Given its linear nature, the sometimes pronounced scarp, and the fact that the trend of the feature fits closely with predicted Okh–NAm motion from global Euler vectors, we suggest that this is evidence of a recently active, mostly strike-slip fault with a left-lateral offset, likely to be the Okh–NAm plate boundary. We now present arguments for potentially large earthquakes and ruptures along it.

2.2 Buyunda fan surface and hydrology

Although today the Buyunda river is in a braided channel to the east of the Buyunda fan and is actively incising its earlier fan deposits, the fan surface is composed of several generations of earlier braided channel systems representing earlier courses of the Buyunda river. These have complicated, discordant relationships to one another, but in general they become less distinct and presumably older in a westerly direction (Fig. 3).

One of the most commonly used means to establish fault slip rates in strike-slip regimes are offset markers, such as alluvial channels, terraces or other stable land forms where they cross a fault (e.g. Grapes and Wellman, 1988; Hubert-Ferrari et al., 2002; Hetzel et al., 2002; Rodgers and Little, 2006). It is often hypothesised that some channels may be offset by a single earthquake and simultaneously abandoned by the stream that flows into them. Under these circumstances, a channel will become a passive marker for the current and all subsequent earthquake offsets. However, there are a number of potential problems with this idea. Firstly, the channel may have already been inactive for other reasons, prior to an offsetting earthquake, and associated ages of channel deposits would therefore not be synchronised with the start of offset motion. This is probably only relevant for cases where single earthquake offsets are being measured. In cases where multiple offsets have occurred, the significance of a time delay between abandonment and the beginning of offsets will become less as more earthquakes occur. Secondly, channels may re-establish flow between offset segments in a phenomenon known as dog-legging (Rodgers and Little, 2006), and hence depositional ages within channels will be younger than the timing of offsetting motion. Dog-legging may also occur where a new channel exploits an existing fault scarp along part of its length, causing a deflection in its course which is unrelated to seismic events. The best tectonic offset markers are generally linear features such as edges of incised terraces (Hetzel et al., 2002) or straight segments of a channel. However, in many cases, associating age determinations of sedimentary features with their offsets is problematic. The Buyunda fan inner lobe surface is crossed by many channels which are intersected by the fault scarp. In general, these form abandoned, braided systems of similar character to the present-day Buyunda river (Fig. 3). Braiding leads to continuously curved features, which makes identifying tectonic offsets more difficult. The eastern end of the fan in the area of the larger thermokarst features nevertheless contains a number of channels with straight segments that cross the fault, often almost perpendicular to it, and none of which appear to be offset. We suggest that this region is the youngest portion of the fan surface and was active after the last major earthquake on this fault segment, which obliterates traces of the active scarp. This system is bounded on its western edge by a channel which turns fault-parallel for a distance of ∼350 m, which could be interpreted as a fault offset but actually appears to mark the edge of this particular generation of deposits (Fig. 3).

Further westwards towards the region of the pronounced fault scarp, the braided channels are less distinct in aerial and satellite imagery (Fig. 4). The fault scarp builds a ridge which cuts through drainage. To the south and north of the ridge, aerial and multispectral LANDSAT imagery shows saturated zones and fossil drainage, suggested by the light colours of the satellite image (Fig. 5). This was also confirmed in the field, where we found substantial areas of persistent surface water. Between them, the scarp builds a “dry” zone (Fig. 4), with dryness implied by the dark colours of the satellite image and also confirmed in the field. The hydrology of this region is dominated by outflow from the adjacent Okhotnik river and fan system, and the fault scarp which forms a step in the regional water table. The area directly north of the scarp is a topographic low on the edge of the inner lobe of the Buyunda fan. Water presumably percolates into the scarp area, fed from the Okhotnik river. The step due to the scarp offsets the hydraulic gradient within the fan deposits, leaving the scarp dry and the areas to its north and south saturated. The saturated zones highlight a fossil channel system which formed a pre-scarp drainage system. The channels with higher permeability sediments are distinctly light coloured in satellite imagery (Fig. 5). The fossil channel system drained to the northwest.

At the westernmost end of the scarp and ridge, directly adjacent to lake Rovnoye, there are two small areas of raised topography, visible on the aerial photographs and the DEM (Fig. 5). The southernmost of these forms the main fault scarp at this point as can be seen from fault-normal topographic profiles (Fig. 7). The fault thus passes between the two topographic highs, before terminating and resuming a few metres south along the main scarp. The topographic features both have straight, eastern edges, trending to the north. They also appear as two darker spots on LANDSAT imagery (Fig. 5c), again suggesting an apparent offset. These features are interpreted as channel banks of an earlier north-draining system, the fossil remnants of which can be seen ∼500 m further north (Fig. 4b). The channel banks are cut by the trace of the fault and offset by 62±4 m in a fault-parallel direction, which we interpret to be a measure of fault offset in this location. We suggest abandonment of the channel may have occurred due to the fault scarp and ridge that were formed during earthquakes, blocking and shutting down the existing drainage. Subsequently, new drainage developed parallel to the scarp and began to flow into lake Rovnoye at the scarp's western end (Fig. 5a).

2.3 Buyunda fan age determinations and offset rate estimates

We collected sediment samples from four sites along the scarp for age determinations using both optically and infrared stimulated luminescence of quartz and feldspars (OSL and IRSL) using the SAR (single aliquot regenerative dose) protocol according to Murray and Wintle (2000), as well as organic material for ¹⁴C from one further site (see Appendices A and B for details of the method, sampling and laboratory procedures). Samples came from the region directly adjacent to and north of the scarp from five pits (Fig. 4), although from one pit (sample 5) we only recovered organic material. Samples 1 and 2 are on both sides of the offset channel feature we have identified, at the westernmost edge of the scarp. Samples 3, 4 and 5 are from the broad zone of channel deposits that we can identify from aerial photographs. Samples 1–4 were analysed with both OSL and IRSL. Sample 5 was ¹⁴C only. Sample pits encountered fine–coarse grained, sandy material, with occasional evidence of graded and cross bedding. Small pebbles sometimes formed the base of cross beds. We believe we sampled a mixture of channel or possibly overbank deposits of a fossilised fan-top channel system, probably part of an old course of the palaeo-Buyunda river when it flowed generally to the northwest, in a direct line to its confluence with the Kolyma river. Sample collection and processing procedures are described in the Appendix. As part of the sampling procedure, we also recovered two samples from different faces of several pits, which are referred to as (a) and (b) samples in this paper.

Samples were generally classified as being either well bleached where quartz (OSL) and feldspar (IRSL) ages are consistent, or partially bleached where quartz and feldspar ages differ significantly. In general, feldspar ages are only considered indicative of true ages of channel deposits when they closely match quartz ages (see Appendix for explanation of methodology and data tables). If feldspar ages do not match quartz ages for an individual sample, only the quartz ages are taken to be representative of the true age of the deposit. From the reliable data there is a range of ages (8.85–14.3 kyr) from samples 1–4, with a mean age of 11.6±2.7 kyr (Table A1, Fig. 8). The ages suggest an early Holocene abandonment of this part of the fan and by extension may date the first uplift of the scarp and ridge structure that we suggest reorganised the drainage in this region. These are probably the first genuinely physical age determinations of Quaternary sediments carried out in this region (Patyk-Kara and Postolenko, 2004), and certainly the first employing OSL. Combining the mean age with the associated 62±4 m offset gives a slip rate of 5.3±1.3 mm yr⁻¹, which agrees with the modern-day plate-tectonic estimate of Okh–NAm motion at this point (Sella et al., 2002).

Figure 8Usable luminescence and ¹⁴C age data from the five sample sites along the Ulakhan fault scarp (for locations see Fig. 4). Raw data, including from partially bleached IRSL samples not considered in age determinations, can be found in the Tables A1, A2 and B1. Data are separated into (a) and (b) samples, which refer to separate samples from different sides of the same pit.

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The poorly bleached feldspar samples have a wide range of ages (12.3–45.6 kyr) (Table A2). Poor bleaching reflects the fact that feldspar luminescence has not been reset during the latest transport and depositional episode (see Appendix). It is quite likely that the Buyunda fan sediments have been reworked from other deposits in the Buyunda river system, and it may be that the ages reflect earlier episodes of transport and deposition in other parts of the drainage basin from which the sediments have been reworked, but there is no method available for quantifying this possibility.

¹⁴C dating of sample 5 gives a far younger age than the neighbouring OSL sites. This is not particularly surprising, given the possible ways of introducing organic material into the subsurface long after deposition has occurred. We suggest that the consistency of the OSL results, probably reflecting time since channel abandonment, make it likely that the ¹⁴C age is post-depositional.

2.4 Basin-wide fault and scarp features

The scarp we encountered in 2011 and 2012 is linked to a fault that can be followed across most of the Seymchan–Buyunda basin. Using remote sensing data, we can trace the fault westwards from the alluvial fan (Fig. 3). Aerial photo coverage also overlaps with parts of this region. The fault extends ∼90 km in total to the northwestern edge of the basin where it may also offset Neogene continental clastic deposits. Immediately west of Lake Rovnoye, aerial photographs show several small lakes which may sit between an overlapping en échelon portion of the fault (Fig. 3). A linear trace then runs to the eastern edge of the incised Kolyma river, marked in places by shutter ridges (Fig. 3). Several smaller rivers cross this part of the fault and have built fans across it. Some of the fan edges suggest left-lateral offsets, but this is not consistently obvious. Linking of offset distributary channels (i.e. identifying consistent, left-lateral offsets) from one side of the fault to the other is also difficult, although this is often the case in strike-slip fault systems (e.g. Hubert-Ferrari et al., 2002; Rodgers and Little, 2006).

Where the Kolyma river enters the Seymchan Basin, it emerges from a deeply incised gorge in Jurassic and Triassic bedrock to the south and has incised a delta-shaped region into the basin infill (Fig. 2). The fault is thus not discernable in this region. West of the Kolyma, however, the fault segment re-emerges, approximately in line with the end of the trace to the east of the river and forming the northern boundary of Neogene outcrops on the south side of the basin. The segment finally terminates in what is apparently a second scarp but with the opposite uplift polarity to that on the Buyunda fan (Fig. 9). This second scarp appears to be somewhat enhanced by erosion along the fault trace, but the offset of the basin floor is clear from the fault-normal topographic profiles (Fig. 9). The northern side of the fault is uplifted by up to 3–5 m, just as the southern side is uplifted by a similar amount at the eastern termination of the fault segment on the Buyunda fan. As we discuss in the next section, these two linked scarps and peak uplifts can be related to elastic dislocation models of earthquakes on strike-slip fault segments.

Figure 9Topographic profiles, showing vertical offsets across presumed scarp at the western end of the Seymchan Basin, assumed to mark the termination of the 90 km Ulakhan fault segment. Offsets reach a similar maximum value to the scarp on the Buyunda fan and diminish rapidly to the west, but more gradually, over a distance of ∼5 km, to the east. Sense of offset is reversed relative to the Buyunda scarp (Fig. 7).

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4.1 Seismological and kinematic data

There have been no large earthquakes (>M_w 7.0) on the plate bounding faults of the northwestern portion of Okh within the instrumental seismic record. The most northerly large earthquake on the boundary of Okh (excluding those along the segment of the Pacific subduction zone) was the Neftegorsk event at the northern end of Sakhalin Island, on the Eur–Okh boundary. Otherwise, excepting the M_w 6.7 Illin-Tas earthquake in 2013, which occurred on the Eur–NAm boundary, north of the triple junction with Okh (Imaeva et al., 2015), the largest event in the region was the intraplate M_w 6.4 Artyk event in 1971, which lay within the Okhotsk plate. This lack of data led Hindle et al. (2009) and Hindle and Mackey (2011) to suggest that there were a number of ways to accommodate Eur–NAm convergence by internal and plate boundary strain within northwestern Okh (Fig. 11). These were an effectively rigid, plate-like “extrusion” of the northwestern corner of Okh from between converging Eur and NAm, with the majority of tectonic displacement occurring on the plate bounding faults; a northwestern corner of Okh consisting of a series of blocks, mostly elongated north–south, moving independently of one another by relatively even amounts over many earthquake cycles, and thus no single clear plate-bounding fault. Although some internal deformation is occurring within Okh as shown by the 1971 intraplate earthquake, it is 1 order of magnitude smaller than that expected for full release of plate-tectonic strain according to Hindle and Mackey (2011). GPS data from northwestern Okh are sparse and have been interpreted in a variety of ways (Steblov et al., 2003; Apel et al., 2006). Our field observations on the Ulakhan fault give a first insight into the palaeo-seismology of the region and add important data in this context.

Figure 11Graphic showing two hypothesised modes of tectonic strain release in the northwestern corner of Okhotsk. (a) Region composed of independent blocks acting as independent micro-plates, with average relative slip across them fairly even. This means there is no distinct Okhotsk–North America or Okhotsk–Eurasia plate boundary. (b) Region composed of blocks that, although they can slip relative to one another, are mostly “stuck together” by compressive force of converging Eurasia–North America. In this case, the behaviour of northwest Okhotsk is plate-like, even if there is some intraplate deformation.

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4.2 Palaeo-seismology, earthquake recurrence and seismic hazard

The fault scarp we encountered requires a recent earthquake or series of earthquakes of large magnitude and also forms part of a single 90 km fault segment that we can trace across the Seymchan–Buyunda basin. The opposite uplift polarities at the likely tips of this segment are a morpho-tectonic signature probably uniquely explained by rupture or repeated ruptures on a single fault segment, as suggested by elastic dislocation modelling. The magnitude of uplift implied by the Ulakhan fault scarp over ∼11.5 kyr also matches well with that predicted for the combination of a 90 km fault segment and the slip magnitude available due to plate-tectonic strain accumulation in this time period (Hindle and Mackey, 2011).

Our interpretation of the field observations has several implications. It confirms a potentially significant seismic hazard in the region, with a likelihood of ≥M_w 7.5 earthquakes occurring within the Seymchan Basin (the 90 km length 10 km deep 15 m slip event modelled in this paper is equivalent to an M_w 7.7 earthquake), and hence affecting both populated areas and large infrastructure, in particular the Kolyma hydro-electric dam located at Ust Srednekan (Fig. 2). It firmly constrains the location of the plate boundary to follow the trace of the Ulakhan fault, and suggests the slip and strain partitioning due to plate-tectonic motions is concentrated ($>\mathrm{90}\mathit{\%}=\mathrm{5}$–6 mm yr⁻¹) on the plate boundaries. This in turn implies that the internal strain of the northwestern Okhotsk plate is confined to the release of small amounts (probably <0.5 mm yr⁻¹) of accumulated slip. This may mean that the largest possible intraplate earthquakes are no bigger than the M_w 6.4 Artyk earthquake of 1971, although ultimately this will also depend on their frequency.

The wider question of recurrence times of large earthquakes on individual fault segments can also be partly addressed by our new results. Hindle and Mackey (2011) considered two possible scenarios for strain release along the plate boundaries of Okh, whilst assuming that rigid, plate-like extrusion occurred. In the first, strain was only seismically released along the Okh–NAm boundary (∼1150 km total length). This was considered a possibility due to the absence of any seismicity, or indeed any clearly defined structure for the plate boundary, along Eur–Okh, which would creep aseismically instead. In this case, the average recurrence times for large earthquakes on any segment of the Okh–NAm boundary were estimated to lie between ∼0.7 and 1.2 kyr. The second scenario had seismic strain release occurring along both Okh–NAm and the adjacent portion of Okh–Eur (total fault length ∼2500 km). In this case, recurrence times were estimated at ∼3.0–4.9 kyr. The lower estimate was based on average earthquake sizes M_w 7.6–7.8. The 3 kyr recurrence interval, with 62±4 m total slip and a suggested age for the offset channel of ∼11.5 kyr for the Seymchan segment of the Ulakhan fault, would give four earthquakes of average slip ∼15 m. Assuming a 15 km rupture depth and a 90 km length gives M_w 7.7 per event.

4.3 Earthquake size and fault dimensions

One of the key questions in earthquake seismology is the nature of any relationship between rupture length and average fault slip. Wells and Coppersmith (1994) analysed a large number of earthquakes from around the globe, and according to their empirical formulae, a single earthquake on a 90 km long fault segment should yield an average ∼1.9–2.8 m slip. Our estimate of ∼15 m slip in a single event on the Ulakhan fault seems large in this context. However, the natural example of the 1855 M_w 8.1 Wairarapa earthquake in New Zealand, which has a relatively well-constrained rupture length of ∼145 km and average slip ∼12–16 m, shows that much higher displacement–length ratios for strike-slip faults are possible (Rodgers and Little, 2006; Grapes, 1999). The Wairarapa fault is interesting as an analogue for the Ulakhan fault in several other ways. Studies have shown it has a Holocene slip rate of ∼6–12 mm yr⁻¹, broadly comparable to that suspected for the Ulakhan, and is mostly undergoing strike-slip displacement (Wellman, 1972; Grapes, 1999). There have also been a sequence of large earthquakes (∼11) on this segment of the Wairarapa through the Holocene, demonstrated by differential uplift of a series of river and beach terraces adjacent to the fault (Grapes, 1999). In general, the Wairarapa fault provides a well-constrained example of the behaviour we hypothesise for the Ulakhan.

A comparison with the Wairarapa fault scarp, with a known source age, relatively well-constrained magnitude and similar kinematics, is also interesting for our study. The Wairarapa fault has multiple offset terrace levels, giving a high-resolution earthquake “stratigraphy” in the landscape and confirming the repeated Holocene ruptures on the segment. These terraces are due to a longer-wavelength landscape uplift pattern around the fault of up to 5 m per earthquake over a wide area (maximum terrace uplift today ∼40 m). This broader uplift pattern is the main driver of terrace formation and abandonment. The scarp from the 1855 earthquake shows a 1–2 m vertical offset and remains visible in many places today (Rodgers and Little, 2006; Grapes, 1999). Elastic modelling of the Wairarapa earthquake (Darby and Beanland, 1992) has suggested a listric fault geometry, partly to account for the broader uplift field. The Ulakhan fault may also be creating uplifted fluvial terraces in a similar way. However, it is difficult to separate tectonic from glacio-eustatic and other base-level-related signals. More generally, the Holocene behaviour of the Seymchan–Buyunda segment of the Ulakhan fault seems to be quite well modelled by a simple vertical strike-slip fault. However, further analysis is probably required in this context.

4.4 Large-scale tectonics

An interesting aspect of the northwestern corner of Okh is its tectonic situation, as a narrow sliver of a small plate caught in compression between much larger converging ones (Eur and NAm) (Fig. 11). Despite the convergent motion of Eur and NAm, the resultant motion along the boundaries of Okh is generally believed to be strike-slip with northwestern Okh moving towards the south, perpendicular to convergence (Cook et al., 1986; Hindle et al., 2006). Due to the proximity of the Eur–NAm Euler pole to the region, the rates of convergence, and hence overall rates of slip on boundaries, are low (∼5 mm yr⁻¹). There are few, if any, other places on earth directly comparable to this. In terms of deformation rates, northern China is broadly similar (Liu et al., 2011). However, northern China is a zone of intraplate deformation. It is also the place with the longest historical record of seismicity in existence, which has allowed unique insights into the nature of slowly deforming regions, faulting and seismicity (Liu et al., 2011). It appears that northern China is composed of a system of linked faults across the plate interior, and these move to some degree in coordinated fashion (Liu et al., 2011). It is only possible to establish this due to the 2000-year record of earthquakes there. By contrast, our work suggests that northwestern Okhotsk is more plate-like with slip concentrated on discrete plate bounding faults, even if there may be relatively large intraplate earthquakes occurring too. It is thus interesting that plate-like behaviour can apparently persist into the realm of very low deformation rates (<5 mm yr⁻¹). At the same time, the Ulakhan fault system may exhibit similar long-term behaviour to much faster slipping strike-slip faults. The North Anatolian Fault (NAF) slips at 23 mm yr⁻¹ and has a length of ∼1000 km (Stein et al., 1997), a length broadly similar to the Ulakhan system. The NAF is also segmented, and sequential earthquake migration over longer time periods on different segments has been observed within historical records (Stein et al., 1997), in a similar fashion to that now postulated at much slower rates along the Ulakhan fault.