Continuous GPS and broadband seismic monitoring have revealed a variety of disparate slip patterns especially in shallow dipping subduction zones, among which regular earthquakes, slow slip events and silent quakes [Dragert et al., 2001; Hirose et al., 1999]. The present understanding of these slip patterns is based upon numerical simulations that impose ad hoc values of the rate and state parameters a and b [Liu and Rice, 2005; Liu and Rice, 2007; Shibazaki and Iio, 2003] derived from the dependence of a and b with temperature [Blanpied et al., 1998]. Slow slip events are sometimes accompanied by Non Volcanic Tremors (NVT), which origin remains unclear [Rogers and Dragert, 2003]. The physical origin of NVT is poorly understood, being either proposed to be triggered by fluid movements [Katsumata and Kamaya, 2003; Obara, 2002] or related to some frictional processes along the subduction interface [Ide et al., 2007; Shelly et al., 2007]. Neither explanation is complete. If fluids are at the origin of tremors, then tremors should be recorded up-dip of the locked zone, where the subducted lithosphere is known to be fluid-saturated. If tremors do find their origin in some frictional process, then we should record NVT not only down-dip the locked zone, but all along the subduction zone. Whatever the process at the origin of NVT, the fact is that they are mostly associated with SSE along subduction zones, suggesting a common origin to both phenomenons. The understanding of SSE is incomplete. Pressure and temperature (P & T) increases with depth are invoked to explain the changes of slip patterns down dip the subduction zone [Schwartz and Rokosky, 2007]. Aqueous fluids released from subsequent metamorphic dehydration reactions (enhanced by P&T changes) have been proposed to play an important role in causing slip transients and NVT [Obara et al., 2004]. From the numerical point of view, P&T changes are used to establish the profile of Rate and State friction parameters a and b with depth [Liu and Rice, 2005; Liu and Rice, 2007]. b-a is tuned to control the stable/unstable behaviour of the subduction interface, being positive or negative respectively. The depth of the transition zone is set up according to the temperature dependence of b-a. This dependence was experimentally determined for a wet granite gouge [Blanpied et al., 1998]. Other studies impose small but negative (b-a) values at the transition zone to reproduce the change in slip pattern. In this latter case, the conditional stability of slip is insured by either a stiffness that is greater than the critical one [Mitsui and Hirahara, 2006] or by a plastic increase of the critical slip distance dc [Shibazaki and Iio, 2003]. In all of these models, the subduction interface is imposed to slip at a constant tectonic velocity below the transition zone. Numerical models of friction applied to subduction zones teach us that the transition between earthquakes and SSE occurs down dip the locked zone, where the slip becomes conditionally stable. However, the same situation for stability exists also up-dip of the locked zone [Scholz, 1998] where no SSE has been observed so far. The processes at the origin of SSE must explain this difference in the slip pattern above and below the locked zone, respectively. The occurrence of NVT is not investigated by these numerical models.
 In the following, we investigate the influence of cumulative slip and ageing of the contact interface on the occurrence of SSE and NVT. The cumulative slip along subduction zones is among the largest on Earth: indeed, a portion of the subducted lithosphere slips over hundreds of kilometres. During this slip, two main processes drive the change in the contact interface: 1/the sediment input in the subduction factory that constitutes a highly deformable contact interface; 2/P & T increases, known to drive changes in rock deformation from elastic brittle to plastic creep behaviours. We have devised a friction experiment (Figure 1) that is aimed at reproducing the main features of a natural subduction zone. To recover P & T effects on rock deformation, we allow for plastic deformation to be effective over the time scale of our friction experiment by using a salt slider [Shimamoto and Logan, 1984; Shimamoto, 1986; Voisin et al., 2007]. The slider, an analogue to a portion of the subduction plate, slides against a flat glass surface which represents the overriding continental lithosphere. The slider is pushed at a constant velocity, equivalent to the tectonic velocity. We follow the displacement of the slider through time, as if we were moving along with the buried lithosphere (Figure 1). We record the Acoustic Emission (AE) induced by the slip of the slider.
 The slip pattern of the slider is observed to evolve continuously with the cumulative displacement. Figure 2 presents four excerpts of this continuous change, taken for different stages of cumulative slip. We observe a change in the frictional behaviour of the slider, from unstable (stick-slip like) to stable slip, passing through quasi stable smooth oscillations. The beginning of the experiment is characterized by large stick-slip events (Figure 2, snapshot 1) which amplitude gradually decreases as the slider enters a smooth oscillations sliding regime (snapshots 2–3). The slip pattern of the slider eventually reaches the continuous sliding regime at the imposed driving velocity (snapshot 4). If the amplitude of slip events is decreasing with the cumulative displacement, the duration of slip episodes increases with the cumulative slip. The stick-slip episodes are characterized by a fast stress release (<0.05 second, limited by the sampling frequency), while the duration of the smooth sliding oscillations is about 30 seconds.
 In a previous study, we reported on the change in the contact interface geometry with cumulative displacement [Voisin et al., 2007]. The change in slip pattern of the slider is accompanied by the development of a striation pattern in the direction of sliding, a decrease in b-a, and an increase in dc. Here we record the AE associated with the slider slippage and track any change in the acoustic recordings in relation with the change in the contact interface. Figure 3 presents three AE records taken after different increasing cumulative slips. The amplitude of AE signals is decreasing with the cumulative displacement. On the contrary the duration of AE signals increases with the cumulative displacement. The envelope of AE signals is evolving as well. The three examples show a transition from strong impulsive signals to a succession of smaller and longer signals, made of distinct acoustic events. Acoustics of friction at the scale of 1 square centimetre is generally related to the surface roughness [Akay, 2002]. Recording the AE at high frequency during the friction experiment provides a way to resolve the processes of ageing going on at a lower scale of friction: the contact asperity scale. In our experiments, the progressive evolution of the acoustic signals is related to the contact interface changes and the development of the striation pattern. The records of AE throughout the experiments reveal a progressive change from impulsive events to smaller and longer signals made of numerous acoustic events. It possibly reproduces the in-situ change from earthquake seismic signals to NVT signals observed in subduction zones. Our experiments argue for slow slip events (SSE) and non volcanic tremors (NVT) being two manifestations of a single friction process, seen at two different scales. These experimental results may shed a new light on both the slip and seismic patterns along the subduction zones. In our experiments, tremor like signals are emitted by unstable slip at the contact asperity scale (shear failure asperities) occurring during the slider slow slip event. Ageing of the contact interface with cumulated displacement does occur along the subduction interface, driving the change from regular to slow to silent earthquakes. Subduction zone NVT appear as a local recollection of the unstable frictional behaviour occurring during the slippage of aseismic slow or silent events down dip the subduction zones [Shelly et al., 2006]. The occurrence of slow and silent events, possibly twined to NVT is possibly linked to the amount of cumulated slip undergone by the deformable contact interface. This might explain why neither SSE nor NVT are recorded up-dip of the locked zone, where the accumulated slip is too small.
 Our experimental results suggest that earthquakes, slow and silent events pertain to a continuum of slip patterns driven by the ageing of the subduction interface with cumulated slip. Estimates of the cumulated slip required to observe slow or silent events on actual subduction zones are given by the depth of these events and the dip angles of subduction zones. Compiling data from Kato  we derive a value for cumulated slip of 70 to 230 km, with a mean value of 130 km. Using the appropriated tectonic plate velocities [Kato, 2003], the necessary time for these slow and silent slip events to emerge is in the 1.5–4 106 yr range, with a 3 106 yr mean value. Although the cumulative slip may be necessary to generate slow slip and tremors, it does not appear to be a sufficient condition in real Earth. As an example, subduction in NE Japan has a large cumulative slip but has not been observed to generate tremors so far. Therefore, a combination of conditions (temperature, pressure, fluids, and cumulative slip) might be required to grasp a complete understanding of the subduction slip patterns and tremors.
 Allowing deformation of the contact interface to interfere with friction reveals a continuum of slip patterns. Earthquakes, slow events, silent quakes and continuous sliding appear as different aspects of a holistic process. The ageing of the contact interface with cumulated displacement provides a global framework to capture the occurrence of the different slip patterns and seismic signals along subduction zones. Considering the cumulative displacement as a sine qua non condition for the occurrence of SSE and NVT explains the absence of these latter above the locked zone. Our experimental results are consistent with and rationalize a posteriori: (i) the modelling of aseismic slip transients by a decrease in b-a [Liu and Rice, 2005] and an increase in dc [Shibazaki and Iio, 2003]; (ii) the hypothesis that silent slip and NVT pertain to one and unique phenomenon of friction; (iii) the hypothesis that NVT are local reminiscence of frictional instabilities in these aseismic slip transients [Shelly et al., 2007].