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Minor thrust fault developed in Ordovician interbedded limestones & shales in Kentucky, USA.
This outcrop is in the famous Cincinnatian Series of the tristate area of Ohio-Kentucky-Indiana. Rocks in the Cincinnatian were deposited in relatively shallow marine facies during the Late Ordovician. The Cincinnatian succession is mostly interbedded limestones and shales. Most of the limestones are event beds (= tempestites), deposited during ancient storms.
The gash extending from upper right to lower left is a minor thrust fault. It is developed in the Bellevue Limestone and Fairview Formation. The fault acted as a conduit for groundwater, which dissolved out a small cave along the strike of the fault (see: www.flickr.com/photos/jsjgeology/31949022868).
Thrust faults are low-angle reverse faults - they form by compressional stress. Thrust faults involve the hanging wall moving upward and the footwall moving downward.
Stratigraphy: Bellevue Limestone over Fairview Formation, Maysvillian Stage, middle Cincinnatian Series, Upper Ordovician
Locality: Maysville West upper cut - roadcut on the southeastern side of Rt. 62/Rt. 68, just south of bridge over Lawrence Creek & south of the Harsha Bridge over the Ohio River, northern Kentucky, USA (~vicinity of 38° 40’ 04.23" North latitude, 83° 48' 07.08" West longitude)
The San Andreas Fault, here exposed on the floor of the Carrizo Plain in one of the most desolate and least-visited regions of California. Note the offset streams cutting across the fault. On the far side is the Pacific plate and on the near side the North American. It's a right-lateral fault, meaning the other side of it is moving to the right, on whichever side you stand. The Pacific side is moving to the northwest in a motion geologists call "right step." Streams that once flowed straight across the fault now step to the right before they continue. These steps are recent. The plate below has moved hundreds of miles in the last two dozen million years. One study says stream channels were offset up to 50 feet in the 1857 Fort Tejon quake, one of the largest in historic time. This section of the fault raises the Elkhorn Scarp through the Elkhorn Hills. The most spine-like segment is also called Dragon's Back
A cut-and-polished chunk of the Triassic New Oxford formation from Frederick, Maryland. This breccia is the product of faulting during the failed Triassic rift that created the down-dropped Frederick valley. It includes mostly angular Cambrian limestone and quartz fragments in a red mudstone matrix. This stuff was jokingly nick-named Rosie's Dinerite because at the time (before the area became completely built up and obliterated by progressive urbanization) there were some exceptional outcrops of it behind Rose's Diner on Route 40 just west of Frederick.
From the collection of Harrison Mayes' signs on display at the Museum of Appalachia in Norris, TN.
Jacob. . . K is Flickr's resident scholar on Mr. Mayes.
I think it was my fault when I originally took these two pics in 2002. Maybe I didn't rewind the film all the way or something before taking the next shot? See notes on what these two pics were supposed to be.
Taken with a Vivitar junk camera Here is a photo of the camera, its the transparent blue one, I found this roll of film in my TV cabinet that was never developed, so I got it developed last weekend.
OH, and how does Flickr know that this roll of film was from 2002? I got them developed and put on CD at Wal Mart. Or is 2002 just the date the photo scanner was made?
another take on the same parking lot where my dentist's office is (was).
iPhone
stripes: www.flickr.com/photos/guyr/sets/72157627235289373/with/69...
The light from my room, while focused on closer imperfections.
Taken with a Fuji Finepix XP10. Actually, taken from a still from the Fuji's HD video.
This image shows part of the southeastern flank of Pavonis Mons. Surface lava flows run down hill from the top left of the image to the bottom right. Perpendicular to that trend are several linear features. These are faults that encircle the volcano and also run along the linear trend through the three Tharsis volcanoes.
This image illustrates how subsurface lava tubes collapse into the free space of the empty tube. Just to the top of the deepest depression are a series of circular pits. The pits coalesce into a linear feature near the left side of the deepest depression.
The mode of formation of a lava tube starts with a surface lava flow. The sides and top of the flow cool faster than the center, eventually forming a solid, non-flowing cover of the still flowing lava. The surface flow may have followed the deeper fault block graben (a lower surface than the surroundings).
Once the flow stops there remains the empty space lower than the surroundings, and collapse of the top of the tube starts in small pits which coalesce in the linear features.
This martian scene spans 18 x 62 kilometers (11 x 38 miles). To see where on Mars this area lies, and to download high-resolution versions of the image, go to bit.ly/2xW0uNx
See the Red Planet Report at bit.ly/14KXe4O for updates on Mars research and exploration. For more about Mars geology, check out the Mars-ePedia: bit.ly/1fnXbhw
For the latest THEMIS Mars images as received by mission scientists, see bit.ly/1d6HA7o . To learn more about the THEMIS camera and its Mars images, see bit.ly/13YOfgm .
This image is in the public domain and may be republished free of charge, but if used it should be credited as NASA/JPL-Caltech/Arizona State University.
Pavonis Mons is one of the three aligned Tharsis Volcanoes. The four Tharsis volcanoes are Ascreaus Mons, Pavonis Mons, Arsia Mons, and Olympus Mars. All four are shield type volcanoes. Shield volcanoes are formed by lava flows originating near or at the summit, building up layers upon layers of lava. The Hawaiian islands on Earth are shield volcanoes. The three aligned volcanoes are located along a topographic rise in the Tharsis region. Along this trend there are increased tectonic features and additional lava flows.
Pavonis Mons is the smallest of the four volcanoes, rising 14 km above the mean Mars surface level with a width of 375 km. It has a complex summit caldera, with the smallest caldera deeper than the larger caldera. Like most shield volcanoes the surface has a low profile. In the case of Pavonis Mons the average slope is only 4 degrees.
NASA's Mars Odyssey spacecraft has spent over 15 years in orbit around Mars, circling the planet more than 69,000 times. It holds the record for longest working spacecraft at Mars. THEMIS, the IR/VIS camera system, has collected data for the entire mission and provides images covering all seasons and lighting conditions.
Over the years many features of interest have received repeated imaging, building up a suite of images covering the entire feature. From the deepest chasma to the tallest volcano, individual dunes inside craters and dune fields that encircle the north pole, channels carved by water and lava, and a variety of other feature, THEMIS has imaged them all.
For the next several months the image of the day will focus on the Tharsis volcanoes, the various chasmata of Valles Marineris, and the major dunes fields. We hope you enjoy these images!
My daughter went to a special preview showing of the film tonight.
They were filmed watching it, she said she was one of the loudest cryers!
The fault that has just appeared on my TV. Those lines appear each time a scene changes and gradually fade out where the picture is static.
It's only on the composite input (which is where my DVD player is attached) and only in certain aspect ratios. Need to investigate if the problem is with the DVD player or the TV.
All bloody annoying though.
Metamorphic rocks result from intense alteration of any previously existing rocks by heat and/or pressure and/or chemical change. This can happen as a result of regional metamorphism (large-scale tectonic events, such as continental collision or subduction), burial metamorphism (super-deep burial), contact metamorphism (by the heat & chemicals from nearby magma or lava), hydrothermal metamorphism (by superheated groundwater), shear metamorphism (in or near a fault zone), or shock metamorphism (by an impact event). Other categories include thermal metamorphism, kinetic metamorphism, and nuclear metamorphism. Many metamorphic rocks have a foliated texture, but some are crystalline or glassy.
Serpentinite is a low- to high-grade metamorphic rock formed by alteration of olivine-rich peridotites (dunites - ultramafic, phaneritic, intrusive igneous rocks). Metamorphism of olivine in the presence of water results in the formation of the mineral serpentine (Mg3Si2O5(OH)4). A metamorphic rock composed principally of serpentine is thus a serpentinite.
Serpentinite has a mottled greenish color, often has the look & feel of hard candle wax, and ranges in texture from crystalline to “foliated”. Many serpentinites have a foliated look to them, but it’s really not due to an planar alignment of crystals. The appearance of “foliated” serpentinites is really the result of extensive development of slickenlined surfaces.
Many serpentinites also have a small component of magnetite that is usually significant enough to feel a slight tug when a magnet is placed next to the rock. Some serpentinites have "veins" of white asbestos (= chrysotile serpentine).
Many Precambrian greenstone belts have significant occurrences of serpentinites. Slices of dunitic mantle caught up in orogenic belts by obduction (= ophiolites) are often serpentinized. Sometimes, mantle peridotite masses that were caught up in rising magmas have been serpentinized (for example, in kimberlites & lamproites).
The serpentinite outcrop seen here is in New England. This is part of the East Dover Ultramafic Body in the Green Mountains of Vermont. The unit is part of the extensive North American Ultramafic Belt, an ophiolite that was originally dunitic mantle material tectonically emplaced during the Taconic Orogeny in the late Middle Ordovician (sensu traditio), about 460 million years ago.
At this site, the rocks are somewhat weathered, partly serpentinized dunites (antigorite partially replacing forsterite olivine + some chromite).
Locality: roadcut on the northern side of Dover Hill Road, just east of the town of East Dover, southern Vermont, USA (vicinity of 42° 57' 00.70" North latitude, 72° 45' 44.33" West longitude)
Crystal Springs and San Andreas lake visible in the distance. Los Trancos is an unusually high spot along the fault line.
Reverse fault in inch-scale layered plagioclase feldspar & pyroxene in the Precambrian of Montana, USA.
Southern Montana’s Beartooth Mountains has one of the few platinum mines in North America. There, platinum and palladium are mined from the 2.71 billion-years-old Stillwater Complex, a classic example of an LLI (large, layered igneous province). LLIs are large intrusive bodies that display large-scale and small-scale layering, even including cross bedding, ripples, graded bedding, channelforms, and other sedimentary-like features. The Stillwater originated as a large subsurface mass of slowly cooling magma. As various minerals crystallized, they settled to the bottom of the magma chamber - this resulted in layering. Igneous rocks that formed this way have a cumulate texture. Currents in the still-liquid portions of the magma chamber produced the sedimentary structures mentioned above. Most of the Stillwater displays only large-scale layering.
The rocks in the Stillwater are mafic and ultramafic, intrusive igneous rocks. Common lithologies include gabbro, norite, harzburgite, anorthosite, troctolite, chromitite, pyroxenite, and dunite. Portions of the Stillwater have been metamorphosed. Olivine is the most commonly altered component - it's usually been metamorphosed to serpentine.
The main platinum (Pt) and palladium (Pd) occurrence is in the Johns-Manville Reef (J-M Reef), an interval in the lower part of the Lower Banded Series. The Pt and Pd occur in intercumulate sulfides, typically pyrrhotite (Fe1-xS) and chalcopyrite (CuFeS2). Platinum ores in the J-M Reef are principally sulfidic anorthosites, but other lithologies also occur. The J-M Reef is the highest grade deposit known for platinum-group elements (PGEs).
The outcrop seen here does not have platinum ore. The layering consists of alternating bands of plagioclase feldspar and pyroxene. The layering was originally horizontal; Stillwater Complex rocks have been structurally tilted by mountain building.
The band from lower left to upper right is a reverse fault. The fault zone has drag folds above and below that show the sense of displacement.
Stratigraphy: Lower Banded Series, Stillwater Complex, Neoarchean, 2.71 Ga
Locality: roadcut along West Fork Stillwater Road (= Forest Service Road 2846), near & above the Stillwater Mine, Beartooth Mountains, southern Montana, USA
Wasserbillig is a lovely village on the River Mosselle. It has territory in France, Luxembourg and Germany. A tax man's nightmare!
The Salton Sea area is one of the southernmost locations where it is possible to see the trace of the San Andreas fault. It is not as clear as in the Carrizo Plain but it is possible to follow an alignment in the field that marks the boundary between rocks of different colors. In this picture, taken while looking south along the fault, the orange rocks are west of the fault while the tan badlands in the background are east of the fault. Of course the ephemeral streams that cut through these valleys are not bothered by the tectonic history of the area and carry their sediment across the fault and onto the Salton Sea depression.
Mecca, California