On 31 August a new eruption began from the same fissure and is still ongoing at the time of writing. After 4 September the movement associated with the dyke was minor, suggesting an approximate equilibrium between inflow of magma into the dyke and magma flowing out of it feeding the eruption. Minor eruptions may have occurred under Vatnajškull; shallow ice depressions marked by circular crevasses (ice cauldrons) were discovered in the period 27/08-07/09, indicating leakage of magma or magmatic heat to the glacier causing basal melting ( Fig. 1 and 2b). On 5 September, aircraft radar profiling showed that the ice surface in the centre of the B ‡r!arbunga caldera had subsided 16 m relative to the surroundings, resulting in a 0.32±0.08 km 3 subsidence bowl ( can be compared to a 1 day interferogram over the ice surface spanning 27 -28 August (Fig. 1), that has maximum line-of-sight (LOS) increase of 57 cm, indicating 55-70 cm of subsidence, during 24 hours. From 24 August to 6 September 16 M≥5 earthquakes occurred on the caldera boundary.Over 22000 earthquakes were automatically detected 16/08-06/09 2014, 5000 of which have been manually checked. Four thousand of these have been relatively relocated, defining the dyke segments. Ground deformation in areas outside the Vatnajškull ice cap, and on nunataks within the ice cap, is well mapped by a combination of InSAR, continuously recording GPS sites, and campaign GPS measurements. The GPS observations and analysis give the temporal evolution of the three-dimensional displacements used in the modelling (Fig. 1). Interferometric analysis of synthetic aperture radar images from the COSMO-SkyMed, RADARSAT-2 and TerraSAR-X satellites was used to form 11 interferograms showing LOS change spanning different time intervals (Supplementary Fig. 2). The analysis of seismic and geodetic data is described in Methods.Initial modelling of the dyke, with no a priori constraints on position, strike or dip, show the deformation data require the dyke to be approximately vertical and line up with the seismicity (Extended Data item 4). We therefore fixed the dip to be vertical and the lateral position of the dyke to coincide with the earthquake locations.We modelled the dyke as a series of rectangular patches and estimated the opening and slip on each patch ( Fig. 3a; see Supplementary Figures 3-4 for slip and standard deviations of opening). We used a Markov-chain Monte Carlo approach to estimate 7 the multivariate probability distribution for all model parameters (Methods) on each day 16/08-06/09 2014 (Fig. 2d). The results suggest that most of the magma injected into the dyke is shallower than the seismicity, which mostly spans the depth range from 5 to 8 km below sea level (see Fig. 2c and Methods). While magma may extend to depths greater than 9 km near the centre of the ice cap, towards the edge of the ice cap where constraints from InSAR and GPS are much better, significant opening is all shallower than 5 km (Fig. 3a). The total volume intruded into the dyke by 28 August was 0.48-0...

Over a 13 day period magma propagated laterally from the subglacial Bárðarbunga volcano in the northern rift zone, Iceland. It created > 30,000 earthquakes at 5–7 km depth along a 48 km path before erupting on 29 August 2014. The seismicity, which tracked the dike propagation, advanced in short bursts at 0.3–4.7 km/h separated by pauses of up to 81 h. During each surge forward, seismicity behind the dike tip dropped. Moment tensor solutions from the leading edge show exclusively left‐lateral strike‐slip faulting subparallel to the advancing dike tip, releasing accumulated strain deficit in the brittle layer of the rift zone. Behind the leading edge, both left‐ and right‐lateral strike‐slip earthquakes are observed. The lack of non‐double‐couple earthquakes implies that the dike opening was aseismic.

Seismic velocity changes correlate with deformation at Kīlauea volcano, advancing noise interferometry as a monitoring tool.

Previous evaluations of the Circumplex Model's curvilinear hypothesis using FACES instruments have yielded conflicting results. A review of the different research procedures and samples used in those investigations revealed that none of the studies had samples large and/or heterogenous enough to test the curvilinear hypothesis adequately. The present study evaluates the curvilinear hypothesis of family functioning and the concurrent validity of FACES III with a sample of optimal size (N = 2,440 families) and diversity. The lack of support for the curvilinear hypothesis in this "greenhouse" sample is explained by different findings for the two FACES III subscales. There was no relationship between the study's measures of well-being and the adaptability subscale and a linear relationship between these measures and the cohesion subscale. Implications of these findings for the continuing use of the FACES III and for the Circumplex Model of Marital and Family Systems are discussed.

An empirical examination of the association between instruments measuring the Beavers-Timberlawn Model of family competence and the Circumplex Model of adaptability and cohesion is presented. Even when triangulated measures were utilized to control for the divergent methods of data collection traditionally employed to operationalize these models of family health, family competence as measured by the Beavers-Timberlawn Family Evaluation Scales was either minimally (mothers) or not associated at all (fathers and children) with balanced and thereby optimal dimensions of adaptability and cohesion as measured by the Family Adaptability and Cohesion Evaluation Scales. Methodological and substantive explanations for the surprising lack of association between measures of these two prominent family assessment models are explored and short- and long-range implications for the growth and practice of family therapy are discussed.