Ringing rocks

Last updated
A child strikes a rock with a hammer at Ringing Rocks Park, Pennsylvania, to generate a distinctive bell sound Ringing Rocks.jpg
A child strikes a rock with a hammer at Ringing Rocks Park, Pennsylvania, to generate a distinctive bell sound

Ringing rocks, also known as sonorous rocks or lithophonic rocks, are rocks that resonate like a bell when struck. Examples include the Musical Stones of Skiddaw in the English Lake District; the stones in Ringing Rocks Park, in Upper Black Eddy, Bucks County, Pennsylvania; the Ringing Rocks of Kiandra, New South Wales; and the Bell Rock Range of Western Australia. Ringing rocks are used in idiophonic musical instruments called lithophones.

Contents

Early investigations

Several early scientists became interested in the ringing rocks; however, none were able to formulate a credible theory on the ringing ability of the rocks or the formation of the boulder fields.

Edgar T. Wherry (1885–1982), mineralogist and botanist, became interested in the ringing rocks while teaching at Lehigh University. Wherry theorized that the ringing was due to the texture of the diabase rocks and that they were supported by other rocks. He identified the boulder fields as a type of felsenmeer. [1]

At the 13th Annual meeting of the Bucks Historical Society in June 1900, Charles Laubach, a noted local geologist and naturalist, described the geology of the diabase "trap" sills with reference to sites such as Bridgeton, Stony Garden, and others. [2]

Benjamin Franklin Fackenthal (1851–1941), local industrialist and trustee of Franklin & Marshall College, became interested with the ringing rocks. Although not a professional geologist, Fackenthal made extensive observations on all of the boulder fields. [3]

In 1965, geologist Richard Faas of Lafayette College took a few of the rocks back to his lab for testing. He found that when the rocks were struck, they created a series of tones at frequencies lower than the human ear can hear. An audible sound is only produced because these tones interact with each other. Although Faas's experiments explained the nature of the tones, they did not identify the specific physical mechanism in the rock which made them. [4]

Sites in Pennsylvania

Locations of several known olivine diabase ringing rock boulder fields Ringing Rock Diabase Locations.jpg
Locations of several known olivine diabase ringing rock boulder fields

Although there have been over a dozen diabase ringing rock boulder fields identified in the Pennsylvania and New Jersey area, [5] [ full citation needed ] the majority are either on private property or have been obliterated by urban development. There are three sites north of Philadelphia which are readily accessible to the public: Ringing Rocks County Park, Stony Garden, and Ringing Hill Park.

Ringing Rocks County Park

Ringing Rocks County Park is a Bucks County park in Upper Black Eddy. [6] Originally, the land was acquired by the Penn family from the Lenape (Delaware Nation) through the infamous 1737 Walking Purchase. It is not clear who made the original land warrant for the area now covered by the Ringing Rocks County Park. On the 1850 property map of Bucks County, the owner appears to be Tunis Lippincott; however, there is no warrantee listing under that name. The earliest published description of the Bridgetown boulder field is found in Davis 1876. [7] The seven-acre boulder field was purchased in 1895 by Abel B. Haring, president of the Union National Bank in Frenchtown, New Jersey. Apparently, Haring wished to protect the ringing rocks from development, and even refused an offer from a manufacturer of Belgian blocks for the right to quarry the stones. [8] [9] On August 22, 1918, the land which contains the Bridgeton Boulder Field was donated by Haring to the Bucks County Historical Society. The grant included 7 acres 8.08 perches of land. A right-of-way was granted by John O. McEntee for access to the park. [3] Later, the land was transferred to Bucks County and operated as a county park. Additional land acquisitions have increased the size of the park to 129 acres.

A postcard depicting a scene from Ringing Hill Park. Ringing Rocks, Pottstown, Pa (64366).jpg
A postcard depicting a scene from Ringing Hill Park.

Ringing Hill Park

Ringing Hill Park is located three miles northeast of Pottstown, Pennsylvania in Montgomery County. The boulder field was first identified in 1742 when a road was cut between Pottstown and New Gosenhoppen (Pennsburg). In 1894, the Ringing Rocks Electric Railway Company was incorporated to purchase the remote Ringing Hill for an amusement park and provide trolley service (1894 to 1932). At the time it was created, the park was approximately 2 miles (3.2 km) out of town. The park was purchased in 1932 by Walter J. Wolf and operated as an amusement park and skating rink. On September 1, 1957, the park was sold to the Ringing Hill Fire Company. [10]

Stony Garden

The Stony Garden, largest of the three public ringing rock boulder fields, is located on the northwest slope of Haycock Mountain in Bucks County, Pennsylvania, near Bucksville. The garden is actually a series of disconnected boulder fields which extend for nearly half a mile, and were formed where the olivine diabase unit crops out along the base of the mountain. The site is undeveloped, and is accessible by a hiking trail which leads from a PA Game Lands parking area on Stony Garden Road. It was purchased by the Commonwealth of Pennsylvania around 1920 as part of PA Game Lands Tract #157, which covers Haycock Mountain. [11]

Buckwampun Historical Society meetings

The ringing rock boulder fields were popular places for meetings of the local Buckwampun Historical Society. Two annual meetings were held at the Bridgeton site (in 1893 and 1898), and one at Stony Garden (in 1890). [9] The Bucks County Historical Society also had a meeting at the Bridgeton site in 1919, the year after they acquired the property. [3]

At the third annual BHS meeting in June 1890 a local physician, John J. Ott of Pleasant Valley, gave a musical performance using boulders taken from the Stony Garden boulder field. The suggestion for the construction of the lithophone was made by the historian William J. Buck. The rocks weighed approximately 200 lb (91 kg) apiece, and apparently Ott was able to change their sound by slightly chipping the boulders. He played several selections using a steel hammer and accompanied by a brass band. "The clear, bell-like tones of the rocks could be heard above the notes of the horns." [3] [8] [9] The tunes included "Home Sweet Home" and a composition of his own entitled "Sounds from the Ringing Rocks" – possibly a takeoff from the 1873 piano music score of the same name. [12]

Formation

These boulder fields in southeastern Pennsylvania and central New Jersey formed from a group of diabase sills in Newark Basin. The sills were formed when stretching of the Earth's crust allowed mafic magma to travel up from the upper mantle inject into the sedimentary basin 200 million years ago (early Jurassic Period). Phenocrysts of two minerals that had crystallized in the upper mantle, olivine and pyroxene, quickly settled out of the magma and collected along the base of the sills. When fully solidified, this crystal-rich layer formed a separate rock unit 10–15 ft (3.0–4.6 m) thick. [13] By the Pleistocene Epoch, the sills had been exposed to the surface by crustal uplift and erosion. During the Pleistocene, outcrops of the olivine diabase were not buried by the glacial sheets; however, they were subjected to severe freezing, or periglacial, conditions. The periglacial environment caused the outcrops to be broken into extensive boulder fields.

Geology

The basal olivine unit is similar to the one found in the Palisades Sill in New Jersey and New York. The olivine diabase unit is significantly harder, denser, and more resistant to weathering than the upper portions of the diabase sill.

Most observers did not make the distinction between the upper "normal" diabase which is found over wide areas, and the thin olivine diabase unit found at the base of the sills which actually produces the ringing rock boulder fields. A main factor in the confusion is the outward appearance of the rocks. Both the normal and olivine diabase rocks are dark grey to black in color. Microscopic examination is often required to identify the differences.

Although the Newark series diabase sills crop out in a belt throughout the length of the Appalachian Mountains, only a narrow band of outcrops in southeastern Pennsylvania and New Jersey develop ringing rock boulder fields. The probable reason is that these areas were at the southern edge of the Pleistocene glaciers, and would have been subject to extreme periglacial conditions. Periglacial boulder fields are a common feature in Pennsylvania and New Jersey.

All of the observed ringing rock boulder fields in southeastern Pennsylvania and New Jersey are a form of felsenmeer (felsenmeer is a German term meaning "sea of rock"). These barren block fields occur in periglacial environments where outcrops of resistant rock are exposed with a slope of less than 25°. Frost wedging breaks up the upper portion of the rock formation, and the slight dip of the field allows the fine weathering materials to be flushed away before soil can develop. Often, the boulders are lifted and rotated by the accumulation of snow and ice, leaving a considerable amount of vacant space between them. The felsenmeer boulder fields form in-situ due to the low-slope angles. In situations where the slope angles are steeper than 25°, gravity tends to move the boulders downhill to form scree or talus slopes. In fields where the angle is too flat, the spaces between the boulders fills with soil and the boulders break down due to weathering.

Because the olivine diabase unit is relatively thin there was an additional requirement for the formation of the ringing rock boulder fields: the olivine diabase unit had to be dipping in the same direction as the slope of the ground surface. This specific dip-slope situation allowed broad expanses of olivine diabase to be exposed and provided enough material to create the fields. In all of the observed boulder fields the structural dip of the unit was approximately 8-10°, and the ground surface slope was <15° in the same direction. Typically this occurred where the olivine diabase unit dipped at right angles into a shallow drainage. Where the olivine diabase does not dip in the same direction as the ground surface there are generally numerous boulders embedded in the soil (boulder colluvium), but no boulder fields.

Ringing ability

There has been a great deal of controversy concerning the ringing ability of the boulders; conversely, there has been an almost complete lack of testing to support the conjectures. Conditions such as size and shape of the boulders and the way that the boulders are supported or stacked certainly influence the sounds that the boulders make but do not in themselves impart the ringing ability.

Although the sound is often described as metallic, it is most likely due to a combination of the density of the rock and a high degree of internal stress. The sound can be duplicated on a small scale by tapping the handle of a ceramic coffee cup.

The iron content of the diabase is often identified as the source of the ringing ability. Actual chemical analysis of the Coffman Hill diabase [13] shows that iron content (as ferric oxide) of the rock ranges from 9% and 12%. Although comparatively high for an average igneous rock (3% is typical for granite), it is within the normal range for a basalt. This point suggests that the iron content is not a primary factor in the ringing ability.

So far, there has been only one published scientific experiment on the source of the ringing ability. In the 1960s, a Rutgers University professor did an informal experiment where specimens of "live" and "dead" ringing rock boulders from the Bucks County park site were sawed into thin slices and then measured for changes in shape. [14] The rock slices were measured with delicate foil strain gauges, which could measure minute changes in size. According to the professor, the dead rocks showed no change after the rocks were sawed; however, the live rocks showed a distinctive expansion or "relaxation" within 24 hours of being cut. This relaxation indicates that the rock was under internal elastic stresses that were released by the mechanical sawing of the rock. The professor went on to make the observation that the live rocks were generally found toward the middle of the boulder fields, where they did not come in contact with soil and the shade of the surrounding trees. He then theorized that the slow weathering rate in the dry "microclimate" of the fields caused the stresses, because the outside skin of the boulders would expand owing to the conversion of pyroxene to montmorillonite (a clay mineral). Boulders along the periphery of the fields weather too quickly and break apart before the stresses can develop.

Although more rigorous testing needs to be done to verify these results, it does suggest strongly that the ringing ability is a direct result of internal stresses. Less likely is the assertion that outside weathering conditions created the stresses. It is very improbable that the expansion of a thin skin around the outside of a large boulder could set up a balance of forces that would create the severe stresses found in the ringing rock boulders. The result of such a situation would be that the outside skin of the boulders would peel or exfoliate, a condition that is virtually non-existent in any of the ringing rocks sites. In addition, the majority of the weathering in the boulders occurs at the exposed top surfaces, not on the bottoms; thus, the stresses would not be balanced. Furthermore, if slow weathering created the stresses, then there would be ringing rock boulder fields in deserts throughout the world, a condition which does not occur.

An important point made in the experiment is the observation that the rock slices expanded when the stress was released. This distinction requires that the rock was under extreme compressive stress, not tension as the slow weathering theory implies.

A more plausible theory is that the elastic stresses remained in the rock when the boulder fields formed, and the slow weathering rate keeps the stresses from dissipating. A possible source of the stresses would likely be the loading stresses from the time when the rock crystallized. The diabase sill formed at roughly 1.2–1.9 miles (2–3 km) beneath the surface. [15] The overlying column of rock creates severe stresses in rocks. The effects of these stresses can be seen in deep mines with a depth of over a mile, where the sudden decompression creates rock bursts. Residual loading stresses would be evenly distributed throughout the boulders. This theory supports the observation that usually less than a third of the boulders in any given field are "live". The stresses are relieved in boulders that have been either mechanically broken or are severely weathered, and therefore no longer ring.

This "relict stress" theory implies that the ringing rock boulders act much like a guitar string. When a guitar string is limp it does not resonate, but a plucked string will provide a range of sounds depending on the level of applied tension. Likewise, a ringing rock boulder will only emit a dull thud if the boulder is de-stressed; however, boulders will resonate at various frequencies depending on the level of residual stress.

The boulders continue to ring when removed from the boulder fields. Myths have been developed by authorities to discourage the theft of boulders from the fields. At the current stage, however, most fields have been picked clean of small portable "ringers", and breaking of large boulders into smaller pieces releases the internal stresses—thus causing them to stop ringing (i.e., breaking a piece off of a large ringing rock will only gain a dead chunk of rock). "Small" ringers found today weigh over a ton and would have to be dragged out of the boulder fields using large equipment.

Weathering textures

Often, the weathering textures in boulders take on the form of channels, grooves, "potholes", "mudcracks", and intense pitting. In some cases, the textures are so distinctive that some geologists refer to them in terms of carbonate rock solution features. [15] Inspection of the boulders reveals that the weathering patterns are not due to any internal variations in the rock, but have been superimposed onto the surfaces. The probable source of these textures was chemical weathering along joint surfaces when the rock was still in place and before the boulders were broken out by frost heaving. [16] The soft weathered portion of the outer surfaces flaked off once the boulders were exposed to the air. Small features on the boulder surfaces became exaggerated as the weathered material was removed, so that adjoining fissures became channels, dents became 'potholes', and old surfaces became intensely pitted.

Ringing Rocks Pluton, Montana

Aerial photograph of the Ringing Rocks Pluton MT RRocks aerial.jpg
Aerial photograph of the Ringing Rocks Pluton

The Ringing Rocks Pluton is located in the mountains of southwest Montana between Butte and Whitehall, and is notable for a large tor of ringing boulders. The pluton is the deep-seated vent for a volcano which erupted 76 million years ago. The pluton is an example of magma mixing in a conduit, specifically between olivine basalt and granitic magmas. Mixing of the magmas created a hybrid rock type which crystallized against the outer wall of conduit. After millions of years of uplift and erosion, the thin walls of hybrid rock were exposed to the surface. During the Pleistocene Epoch, periglacial freezing shattered the high standing walls to form a substantial tor.

Location

Location of the Ringing Rocks Pluton MT RRocks Location.png
Location of the Ringing Rocks Pluton

The Ringing Rocks Pluton is located on the southwestern flank of Dry Mountain in Jefferson County, 15 miles southeast of Butte in T.2 N., R.5 W., sections 4 and 9. Section 4 is included in the Deerlodge National Forest, and section 9 is under the jurisdiction of the U.S. Bureau of Land Management. A distinctive tor is marked on the U.S. Geological Survey Dry Mountain 7½' quadrangle. The NW¼ of Section 9, which includes the tor, was established as the Ringing Rocks Recreation Area by the USBLM in 1964. Access is by a gravel road leading 3 miles north of the Pipestone exit off I-90.

Geology

The Ringing Rocks Pluton is a small-scale intrusive ring complex with a high degree of symmetry. The overall geometry is cylindrical, with an average diameter of one kilometer. The pluton consists of two major units: an inner core of quartz-bearing felsic units with a diameter of 600 meters and an outer mafic unit composed of coaxial concentric layers. In map view, the complex has a bulls-eye configuration. The outer zone of the pluton consists of two alternating mafic hybrid rock types. In chemical analysis the rocks are nearly identical; however, the early stage minerals, olivine and pyroxene, were preserved in one and not the other, giving the rocks sharply different weathering properties. The rock that retained the olivine and pyroxene crystals (OPM) is extremely resistant to weathering and is the material which forms the tors. The altered rock (AM) conversely is very weak and readily breaks down to a coarse soil. The inner felsic core is a medium grained quartz monzonite that gradually grades into granite at the center. The transitional unit between the mafic zone and the felsic core units is completely obscured, and is represented by distinctive low-lying swales. A series of radial dikes punctured the mafic units, beginning in the felsic zone and terminating at the outer border of the intrusion. The dikes are generally 2–4 meters wide where they are in contact with the felsic unit. The composition is highly variable, but for the most part is composed of fine to medium-grained leucocratic monzonite. The dikes become narrower as they extend toward the outer border, and generally taper to less than 0.5 m in width.

Microscopic quench textures in the olivine pyroxene monzonite

There are numerous textures in the hybrid OPM unit which indicate that the rock was rapidly quenched during crystallization.

Crystals of cryptoperthetic orthoclase up to 1 cm in length can be seen in hand specimens throughout most of the OPM units. The cryptoperthite crystals typically show as deep blue flashes, although white and yellow flashes can be seen in rocks nearer to the contacts. The flashes are due to labradorescent internal reflections, sometimes called a moonstone effect. In early reports [17] [18] this mineral was mistakenly identified as labradorite. Cryptoperthite textures form when orthoclase (a feldspar mineral containing both potassium and sodium cations) is quenched very rapidly. Sodium has a much larger ionic radius than potassium does, so during the quench event the sodium ions pop out of the crystal framework. These sodium ions form tiny oriented lenses of albite (sodium silicate feldspar) that are too small to be seen even using a microscope. It is the reflections from these albite laminae that produces the flash.

Apatite occurs as elongated needles. Many of the needles enclose narrow fluid inclusions, giving the crystals the appearance of being "hollow".

Zircon crystals were identified in skeletal frameworks.

Similar intrusions

Igneous geology of the Elkhorn Thrust Plate, southwest Montana MT RRocks elkhorn plate.pdf
Igneous geology of the Elkhorn Thrust Plate, southwest Montana

The Ringing Rocks Pluton is one of several bimodal vent complexes that are located within a 20 km belt east of the main Butte Pluton. Radiometric dating and cross-cutting relationships place most of these intrusions as post-Elkhorn Mountains Volcanics and pre-Butte Pluton. Similar intrusions can be found in the Rader Creek Pluton.

The Ringing Rocks Tor

The pile of loose boulders at the south end of the pluton which contains the ringing rocks is called a tor. The reason the tor developed is that the OPM units are extremely resistant to weathering, and conversely the adjoining AM and ABM units are very weak. As the Dry Creek drainage began to erode the NW corner of the pluton, the softer AM and ABM units were quickly stripped away, leaving vertical thin walls of OPM units standing high above the surrounding landscape. Intense freezing and thawing during the Pleistocene periglacial period slowly shattered the walls, much like breaking tempered glass. The remnants of the OPM walls is the material which formed the tor. At the north end of the pluton the orientation of the OPM units was at an acute angle to the Dry Creek drainage so that the tor there did not develop very well. On the south end, however, the OPM outcrop was nearly at a right angle to the drainage, producing a prominent tor.

Tor at the south end of the Ringing Rocks Pluton MT RRocks tor.pdf
Tor at the south end of the Ringing Rocks Pluton

Ringing properties

Although the rocks are from different geologic settings, the Montana ringing rocks share significant characteristics with the Pennsylvania diabase ringing rocks. These characteristics include being composed of igneous mafic rock types with high percentages of olivine and pyroxene phenocrysts, having the individual boulders isolated from severe weathering by the formation of well-drained boulder fields, and having similar sounds and surface weathering.

The iron content of the olivine pyroxene monzonite (as ferrous oxide) is 7% of the whole rock. [17] [18] As in the Pennsylvania diabase ringing rocks, this point suggests that iron content is not a primary factor in the ringing ability.

Despite the broad public interest in the ringing ability of the ringing rocks, there has not been any actual scientific studies to identify the source of the phenomenon.

Weathering textures

Boulders of the olivine pyroxene monzonite develop odd surface weathering patterns, similar to the textures seen in the Pennsylvania diabase ringing rocks. These textures include channels, grooves, and "potholes".

Bell Rock Range

The Bell Rock Range is a large ultramafic gabbro-peridotite intrusion in the Musgrave Block of Western Australia, near Warburton, 40 kilometres (25 mi) south of the Wingellina community in the Ngaanyatjarra lands. [19] It is composed of massive, heavily indurated intrusive rocks and forms a prominent 15 kilometres (9.3 mi) long range of mountains and hills. The Bell Rock Range is also the site of an exploratory gold mine. [19]

List of sites

See also

Related Research Articles

<span class="mw-page-title-main">Gabbro</span> Coarse-grained mafic intrusive rock

Gabbro is a phaneritic, mafic intrusive igneous rock formed from the slow cooling magma into a holocrystalline mass deep beneath the Earth's surface. Slow-cooling, coarse-grained gabbro is chemically equivalent to rapid-cooling, fine-grained basalt. Much of the Earth's oceanic crust is made of gabbro, formed at mid-ocean ridges. Gabbro is also found as plutons associated with continental volcanism. Due to its variant nature, the term gabbro may be applied loosely to a wide range of intrusive rocks, many of which are merely "gabbroic". By rough analogy, gabbro is to basalt as granite is to rhyolite.

<span class="mw-page-title-main">Mafic</span> Silicate mineral or igneous rock that is rich in magnesium and iron

A mafic mineral or rock is a silicate mineral or igneous rock rich in magnesium and iron. Most mafic minerals are dark in color, and common rock-forming mafic minerals include olivine, pyroxene, amphibole, and biotite. Common mafic rocks include basalt, diabase and gabbro. Mafic rocks often also contain calcium-rich varieties of plagioclase feldspar. Mafic materials can also be described as ferromagnesian.

<span class="mw-page-title-main">Dunite</span> Ultramafic and ultrabasic rock from Earths mantle which is made of the mineral olivine

Dunite, also known as olivinite, is an intrusive igneous rock of ultramafic composition and with phaneritic (coarse-grained) texture. The mineral assemblage is greater than 90% olivine, with minor amounts of other minerals such as pyroxene, chromite, magnetite, and pyrope. Dunite is the olivine-rich endmember of the peridotite group of mantle-derived rocks.

<span class="mw-page-title-main">Amphibolite</span> Metamorphic rock type

Amphibolite is a metamorphic rock that contains amphibole, especially hornblende and actinolite, as well as plagioclase feldspar, but with little or no quartz. It is typically dark-colored and dense, with a weakly foliated or schistose (flaky) structure. The small flakes of black and white in the rock often give it a salt-and-pepper appearance.

<span class="mw-page-title-main">Anorthosite</span> Mafic intrusive igneous rock composed predominantly of plagioclase

Anorthosite is a phaneritic, intrusive igneous rock characterized by its composition: mostly plagioclase feldspar (90–100%), with a minimal mafic component (0–10%). Pyroxene, ilmenite, magnetite, and olivine are the mafic minerals most commonly present.

<span class="mw-page-title-main">Peridotite</span> Coarse-grained ultramafic igneous rock type

Peridotite ( PERR-ih-doh-tyte, pə-RID-ə-) is a dense, coarse-grained igneous rock consisting mostly of the silicate minerals olivine and pyroxene. Peridotite is ultramafic, as the rock contains less than 45% silica. It is high in magnesium (Mg2+), reflecting the high proportions of magnesium-rich olivine, with appreciable iron. Peridotite is derived from Earth's mantle, either as solid blocks and fragments, or as crystals accumulated from magmas that formed in the mantle. The compositions of peridotites from these layered igneous complexes vary widely, reflecting the relative proportions of pyroxenes, chromite, plagioclase, and amphibole.

<span class="mw-page-title-main">Diabase</span> Type of igneous rock

Diabase, also called dolerite or microgabbro, is a mafic, holocrystalline, subvolcanic rock equivalent to volcanic basalt or plutonic gabbro. Diabase dikes and sills are typically shallow intrusive bodies and often exhibit fine-grained to aphanitic chilled margins which may contain tachylite.

<span class="mw-page-title-main">Intrusive rock</span> Magmatic rock formed below the surface

Intrusive rock is formed when magma penetrates existing rock, crystallizes, and solidifies underground to form intrusions, such as batholiths, dikes, sills, laccoliths, and volcanic necks.

<span class="mw-page-title-main">Wichita Mountains</span> Mountains in the US state Oklahoma

The Wichita Mountains are located in the southwestern portion of the U.S. state of Oklahoma. It is the principal relief system in the Southern Oklahoma Aulacogen, being the result of a failed continental rift. The mountains are a northwest-southeast trending series of rocky promontories, many capped by 500 million-year old granite. These were exposed and rounded by weathering during the Pennsylvanian and Permian Periods. The eastern end of the mountains offers 1,000 feet (305 m) of topographic relief in a region otherwise dominated by gently rolling grasslands.

<span class="mw-page-title-main">Tachylite</span> Form of basaltic volcanic glass

Tachylite is a form of basaltic volcanic glass. This glass is formed naturally by the rapid cooling of molten basalt. It is a type of mafic igneous rock that is decomposable by acids and readily fusible. The color is a black or dark-brown, and it has a greasy-looking, resinous luster. It is very brittle and occurs in dikes, veins, and intrusive masses. The word originates from the Ancient Greek ταχύς, meaning "swift".

<span class="mw-page-title-main">Lamprophyre</span> Ultrapotassic igneous rocks

Lamprophyres are uncommon, small-volume ultrapotassic igneous rocks primarily occurring as dikes, lopoliths, laccoliths, stocks, and small intrusions. They are alkaline silica-undersaturated mafic or ultramafic rocks with high magnesium oxide, >3% potassium oxide, high sodium oxide, and high nickel and chromium.

<span class="mw-page-title-main">Komatiite</span> Magnesium-rich igneous rock

Komatiite is a type of ultramafic mantle-derived volcanic rock defined as having crystallised from a lava of at least 18 wt% magnesium oxide (MgO). It is classified as a 'picritic rock'. Komatiites have low silicon, potassium and aluminium, and high to extremely high magnesium content. Komatiite was named for its type locality along the Komati River in South Africa, and frequently displays spinifex texture composed of large dendritic plates of olivine and pyroxene.

<span class="mw-page-title-main">Cumulate rock</span> Igneous rocks formed by the accumulation of crystals from a magma either by settling or floating.

Cumulate rocks are igneous rocks formed by the accumulation of crystals from a magma either by settling or floating. Cumulate rocks are named according to their texture; cumulate texture is diagnostic of the conditions of formation of this group of igneous rocks. Cumulates can be deposited on top of other older cumulates of different composition and colour, typically giving the cumulate rock a layered or banded appearance.

<span class="mw-page-title-main">Igneous intrusion</span> Body of intrusive igneous rocks

In geology, an igneous intrusion is a body of intrusive igneous rock that forms by crystallization of magma slowly cooling below the surface of the Earth. Intrusions have a wide variety of forms and compositions, illustrated by examples like the Palisades Sill of New York and New Jersey; the Henry Mountains of Utah; the Bushveld Igneous Complex of South Africa; Shiprock in New Mexico; the Ardnamurchan intrusion in Scotland; and the Sierra Nevada Batholith of California.

This glossary of geology is a list of definitions of terms and concepts relevant to geology, its sub-disciplines, and related fields. For other terms related to the Earth sciences, see Glossary of geography terms.

<span class="mw-page-title-main">Igneous rock</span> Rock formed through the cooling and solidification of magma or lava

Igneous rock, or magmatic rock, is one of the three main rock types, the others being sedimentary and metamorphic. Igneous rocks are formed through the cooling and solidification of magma or lava.

<span class="mw-page-title-main">Southern Oklahoma Aulacogen</span> Failed rift in the western and southern US of the triple junction that became the Iapetus Ocean

The Southern Oklahoma Aulacogen is a failed rift, or failed rift arm (aulacogen), of the triple junction that became the Iapetus Ocean spreading ridges. It is a significant geological feature in the Western and Southern United States. It formed sometime in the early to mid Cambrian Period and spans the Wichita Mountains, Taovayan Valley, Anadarko Basin, and Hardeman Basin in Southwestern Oklahoma. The Southern Oklahoma Aulacogen is primarily composed of basaltic dikes, gabbros, and units of granitic rock.

<span class="mw-page-title-main">Farmington Gabbro</span>

Located in the Charlotte Belt of North Carolina is the Farmington Gabbro, located in the Mocksville Complex. The Mocksville Complex consist of metamorphosed/unmetamorphosed gabbros, pyroxenites, hornblendites, wehrlites, granites, and diorites. The plutons in this region formed during the Taconic, Acadian, and Alleghanian orogeny starting on the eastern side of Laurentia. These plutons date back to around 400 Ma, consisting of ultramafic, mafic, and felsic rocks but the Farmington Gabbro is the only pluton on the northwest side of the complex that is unmetamorphosed.

<span class="mw-page-title-main">Roosevelt Gabbros</span>

The Roosevelt Gabbros are an intrusive igneous geological formation in southwestern Oklahoma. They are one of two formations recognized in the Raggedy Mountain Gabbro Group, the other being the Glen Mountain Layered Complex. The Roosevelt Gabbros are generally characterized as biotite gabbros, which form many dikes and sills through the older Glen Mountain Layered Complex. They are named after the town of Roosevelt in Kiowa County, Oklahoma.

References

  1. ↑ Wherry, Edgar T. (1912). "Apparent Sun-Crack Structures and Ringing-Rock Phenomena in the Triassic Diabase of Eastern Pennsylvania". Proceedings of the Academy of Natural Sciences of Philadelphia. 64: 169–172. JSTOR   4063462 .
  2. ↑ Laubach, Charles (11 June 1900). "Thirteenth Annual Meeting". Doylestown Intelligencer. Doylestown, Pennsylvania.
  3. 1 2 3 4 Fackenthal, B.F. (1919). "The Ringing Rocks of Bridgeton Township". A Collection of Papers Read Before the Bucks County Historical Society. Vol. 5. Bucks County Historical Society. pp. 212–221.
  4. ↑ Krystek, Lee. "Weird Geology: Ringing Rocks" (Web). Unmuseum. Retrieved 2010-08-16.
  5. ↑ For an extensive inventory of sites, see Pontolillo, J., and Pontolillo, J. (1993) "Ringing Rocks Sites in Pennsylvania and New Jersey" INFO Journal #68.
  6. ↑ "Ringing Rocks Park". Pennsylvania. Archived from the original (Web) on 2006-06-25. Retrieved 2010-08-16.
  7. ↑ Davis, William Watts Hart (1876). The History of Bucks County, Pennsylvania: From the Discovery of the Delaware to the Present Time. Lewis Publishing Company.
  8. 1 2 Humphreys, P.W. (December 1905). "A Trip to Ringing Rocks". The Rambler Magazine. pp. 309–314.
  9. 1 2 3 Sigafoos, Lewis (1935). "Buckwampum Historical and Literary Society". In Fackenthal, B.F. (ed.). Bucks County Historical Society Papers. Vol. 7. Bucks Country Historical Society. pp. 414–419.
  10. ↑ "History of the Ringing Hill Fire Co". Ringing Hill Fire Company. Archived from the original on 2013-01-16.
  11. ↑ "Visiting Bucks County's Other Ringing Rocks: Stony Garden in State Game Lands 157". Uncovering PA. UncoveringPA.com. 2018-12-14. Retrieved 23 August 2019.
  12. ↑ "Sounds from the "ringing rocks"". 1873.[ dead link ]
  13. 1 2 McCray, S.S. (1997). Petrogenesis of the Coffman Hill diabase sheet, Easton Pennsylvania (unpublished B.S. thesis). Easton: Lafayette College.
  14. ↑ Gibbons II, John F.; Schlossman, Steven (December 1970). "Rock Music". Natural History. 79 (10). American Museum of Natural History: 36–41.
  15. 1 2 Sevon, W. D.; Fleeger, G. (1999). Ringing Rocks Block Field: Guidebook. 64th Annual Field Conference of Pennsylvania Geologists. Allentown, Pennsylvania. p. 112.
  16. ↑ Psilovikos, A.; Van Houten, F. B. (1 June 1982). "Ringing rocks barren block field, East-Central Pennsylvania". Sedimentary Geology. 32 (3): 233–243. Bibcode:1982SedG...32..233P. doi:10.1016/0037-0738(82)90051-3.
  17. 1 2 Butler, Barbara (1983). Petrology and geochemistry of the Ringing Rocks pluton Jefferson County Montana (B.A. thesis). Missoula: University of Montana.
  18. 1 2 Johannesmeyer, Thomas (1999). Magma mixing and mingling in the Late Cretaceous Ringing Rocks pluton Jefferson County Montana and implications for the generation of the Boulder batholith (M.S. thesis). Missoula: University of Montana.
  19. 1 2 "West Musgrave". integra mining limited. Archived from the original (Web) on 2010-09-07. Retrieved 2010-08-16.
  20. ↑ Hanauer, David. "Ringing Rocks Park, Bucks County, Pennsylvania". Pennsylvania. Retrieved 2010-08-16.
  21. ↑ "Ringing Rocks Point of Interest".

Further reading

This page is based on this Wikipedia article
Text is available under the CC BY-SA 4.0 license; additional terms may apply.
Images, videos and audio are available under their respective licenses.