El Introduction El Stratigraphy E2 Cambrian System E2 Rome Formation (Lower Cambrian) E2 Honaker Dolomite (Middle and Upper Cambrian) E3 Nolichucky Shale (Upper Cambrian) E4 Cambrian and Ordovician Systems E4 Ordovician System E8 Middle Ordovician limestones E8 Martinsburg Formation E8 Juniata Formation E9 Silurian System E9 Tuscarora Quartzite E9 Rose Hill Formation E9 Keefer Sandstone E9 Tonoloway Limestone E10 Devonian System E10 Rocky Gap Sandstone E10 Huntersville Chert E10 Millboro Shale E10 Brallier Shale Ell Chemung Formation Ell Mississippian System Ell Price Formation Ell Maccrady Shale Ell Greenbrier Limestone E12 Mauch Chunk Group E12 Bluefield Formation E12 Hinton Formation E12 Princeton Sandstone E13 Bluestone Formation E13 Structural Geology and Seismicity E13 Structural Setting E13 Regional Structures E13 Tectonic Evolution E17 Seismicity E18 Mineral Resources E19 Iron E19 Manganese E19 Nonmetallic Resources E19 Fossil Fuels E19 Geologic Hazards E20 References Cited E20

Late Paleozoic depositional trends in the central Appalachian Basin

The current (1996) national probabilistic seismic-hazard maps utilize information about geologic structure and tectonics of the central and eastern U.S. to compensate for uncertainty that arises from the short seismicity record. Geology was incorporated into the maps mainly as seven source zones that are delineated in three distinct ways. The North American stable continental region is divided into two large zones, the sparsely seismic Precambrian craton and the more active Phanerozoic rim. Five other source zones are much smallerqthe Wabash Valley source zone is within the craton, whereas the Reelfoot Rift, eastern Tennessee, Charleston, and Charlevoix source zones are in the Phanerozoic rim of the continent. We document these zones and explain and justify their use. The seven zones provide a foundation from which we suggest a criterion for including more geology in future maps.

Geology in the 1996 USGS Seismic-hazard Maps, Central and Eastern United States

Time histories of hypothetical earthquakes, along with their peak-particle accelerations, and 0 and 5 percent damped response spectra are developed as guidelines for the seismic design of highway structures and bridges within Kentucky. The time histories are derived through the use of random vibration analyses, and take into consideration the probability of earthquakes from nearby seismic zones, the attenuation of ground motions with distance in the Central United States, and the possibility of a random event occurring outside of the generally recognized zones of seismicity in the area. Suggested peak-particle accelerations, time histories, and response spectra are intended for use at sites where the structure is assumed to be situated at the top of a bedrock foundation. For sites underlain by soils, and in particular for those sites underlain by poorly consolidated soils, it is recommended that site specific investigations be conducted by qualified professionals in order to determine the possibilities of frequency-dependent amplification (including resonance), damping, and soil failure when subjected to the suggested time histories. It should be noted that the seismic data is generated at the county seat and not at the county centroid.

/pdf/source-zones-recurrence-rates-and-time-histories-for-4cdjnk0rtm.pdf

Source Zones, Recurrence Rates, and Time Histories for Earthquakes Affecting Kentucky

A local weakening of the brittle-ductile transition can explain some intraplate seismic zones

Abstract I explore the hypothesis that most intraplate earthquakes and their aftershock sequences are triggered by pore-fluid pressure increases. As proposed in this paper, data from the magnitude 5.7 Virginia earthquake of 23 August 2011 show that this is a two-step process. (1) First, from areas where there is greater than normal meteoric recharge, pore-fluid pressure diffusion by means of Biot slow waves transfers more pore-fluid pressure towards a future hypocentre. Here the cumulation of Biot slow waves produces a steady increase in pore-fluid overpressure until a main shock is triggered. (2) Then, aftershocks occur in the zone reaching from the depth of the main shock to a depth of a few kilometres below the land surface, preferring to localize in a weaker, pervasive anisotropic crustal fabric, in response to locally increased permeability and pore-fluid pressure transients caused by the main shock. The primary corrosive agent responsible for reducing the strength of silicate minerals in this upper crustal zone is water, so that quartz-rich crust tends to have lower values of Poisson's ratio. I show here that increases in pore-fluid overpressure from normal groundwater recharge can start crack dilation leading to fracturing and the creation of new permeability. Previous chemical analyses across the Central Virginia Piedmont that hosted the 2011 Virginia shock show high upper crustal quartz content. This proposed two-step model for a main shock-aftershock sequence explains why intraplate earthquakes are rarely correlated with recognizable brittle faults at the Earth's surface. Supplementary material: A biography of John Costain is available at https://dx.doi.org/10.6084/m9.figshare.c.2854324.v3

Groundwater recharge as the trigger of naturally occurring intraplate earthquakes

/pdf/the-giles-county-virginia-seismic-zone-seismological-results-18pxmco1ty.pdf

The Giles County, Virginia, seismic zone; seismological results and geological interpretations

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The Giles County, Virginia, seismic zone; seismological results and geological interpretations