Subaqueous strombolian eruptions, and eruption-fed pyroclastic deposits in a Paleoproterozoic rifted-arc: Hidden formation, Flin Flon, Canada
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Strombolian eruption
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Pillow lava
Lineation
With development of engineering constructions,such as the Qinghai-Tibet Highway and the Qinghai-Tibet Railway,the slope instability problems in permafrost regions of the Qinghai-Tibet Plateau must be carefully considered.Among the slope instability types,thaw slumping is the most hazardous to engineering projects.The ground temperature data of long-term monitoring in the typical thaw slumping indicates that average ground temperature increases and annual fluctuation of ground temperature are reducing under the thaw slumping.The reason is that the heat flux entering permafrost reduces.Retrogressive erosion data of long-term monitoring in the typical thaw slumping indicates that expanding of the thaw slumping fluctuates along with the ground temperature's annual fluctuation,and expanding mostly takes place in 7～9 months.The maximal expanding appears at the direction of the slope tendency.Forming and developing of the thaw slumping are relative to the permafrost conditions and other outer conditions.The basal conditions of slope disappearing must be considered in engineering treatment.
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To study the deformation characteristics of the thaw slumping body at the alignment of K3035 in permafrost area of Qinghai-Tibet Platean,two deformation monitoring boreholes were instrumented with Geokon-603 clinometers,and one borehole lay in the non-sliding soil body while the other lay in the front part of the slumping soil body.Monitoring results of nearly one year show that the thaw slumping body developed in the slope of small dip angle has obvious deformation and its displacement mainly occurs in shallow soil area and decreases with depth.The monitoring results were verified by numerical simulations.The monitoring data comparisons between the thaw slumping body at the alignment of K3035(southern slope) and that at the alignment of K3057(northern slope) were carried out.With reference to both the leading edge and the rear edge of the thaw slumping body,the deformation of the former thaw slumping body is always greater than that of the latter.While in the slope with no thaw slumping(at the alignment of DK1139 of Qinghai-Tibet railway) the deformation is very limited.The difference indicates that on the one hand excavation is the direct factor causing thaw slumping,and on the other hand,because of thaw slumping,the soil body at the rear edge of the slope which is relatively stable originally will experience relatively large creep.
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The basal portion of the St. Anthony Complex is made up of structural slices 10–30 m thick, with unknown amounts of relative movement between them. The lowest rocks are variably deformed pillow lavas and related rocks with one pervasive foliation. These rocks are overlain by greenschists, phyllonites, and mylonites with up to three planar structural elements developed. At least one of these latter surfaces (the earliest) had formed before the schists were thrust over the underlying pillow lavas. The overthrusting event resulted in deformation of underlying pillow lavas. All deformation occurred under lower greenschist facies conditions. Fold axes in the least deformed rocks have variable orientations, and this variation decreases up-section until axes are parallel and plunge gently eastwards, parallel to the stretching lineation. Parallelism between fold axes and stretching lineation implies rotation of fold axes during progressive deformation and is consistent with the rocks being part of a high-strain zone developed during regional overthrusting from east to west.
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Through an analysis of the recent successive slumping several times in Dadaoshan in the City of Lianyungang, the authors studied and analyzed the formation mechanism and trend of slumping in this area and raised keep away measures from the disasters which might be caused by the follow up slumping。
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ABSTRACT Sandstones of the uppermost Witteberg Group in the Cape fold belt of South Africa exhibit unusual and distinctive soft‐sediment deformation structures. These structures include folds, axial planar cleavage and micro‐fold lineations. Interfering fold patterns and intersecting sets of lineations are indicative of repeated deformation. The sandstones are immediately overlain by glacial and proglacial sediments of the Carboniferous Dwyka Group, indicating that the deformation was related to glaciation. Possible environments of deformation include: (a) subglacial dragging of unconsolidated material, (b) subaqueous slumping beyond the limit of floating ice, and (c) englacial deformation of material incorporated by freezing into the base of the glacier.
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