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Graben often occur side by side with horsts. Horst and graben structures indicate tensional forces and crustal stretching. Graben are produced from parallel normal faults, where the displacement of the hanging wall is downward, while that of the footwall is upward. The faults typically dip toward the center of the graben from both sides.
A graben is a section of crust that has lowered relative to the blocks on either side, which is a result of its bounding faults dipping towards each other. [2] The plural of graben can be either graben or grabens. Graben form low-lying features such as basins and rift valleys. [1] [2] They can be very long relative to their width.
In a reverse fault, the hanging wall displaces upward, while in a normal fault the hanging wall displaces downward. Distinguishing between these two fault types is important for determining the stress regime of the fault movement. The problem of the hanging wall can lead to severe stresses and rock bursts, for example at Frood Mine. [16]
The Graben traces its origin back to the old Roman encampment of Vindobona. The south-western wall of the settlement extended along the length of the present-day Graben and Naglergasse; before the wall lay a trench (Graben). This trench still stood in front of the medieval city walls.
Although sediments arrive primarily from the unfaulted side of the half-graben, some erosion takes place on the fault escarpment of the main border fault, and this produces characteristic alluvial fans where confined channels emerge from the escarpment. [9] Lake Baikal is an unusually large and deep example of half-graben evolution. The lake is ...
The Bresse Graben lies to the east of the Limagne Graben. Rifting started during the Eocene, pausing from the Late Oligocene to Middle Miocene before resuming in the Late Miocene. The eastern margin of the basin was overridden by thrust faults from the Jura Mountains , the leading edge of the Alpine thin-skinned deformation .
The Whakatāne Graben (also Whakatane Graben) is a predominantly normal faulting tectonic feature of the northeastern aspect of the young, modern Taupō Rift in New Zealand. At the coast it is widening by about 7 mm (0.28 in)/year. [ 5 ]
Slickenside formation results in unique roughness on a slip surface. Fault surface roughness (or topography) is characterized by the aspect ratio of asperity height to scale of observation, and this roughness is a key parameter in the study of fault slip. [8]