The general attitude of the formation was determined by tracing the basal sedimentary member and two coarsely porphyritic flows of the volcanic sequence. None of the sedimentary interbeds is continuous enough to serve as a marker horizon.
The structure of the formation is simple. North of the Rose River the porphyritic flows and the sedimentary members dip 15° to 20° E. or SE. The western boundary of the formation is the outcrop of the pre-Catoctin erosion surface and is marked by a few inches to 150 feet of sedimentary rocks containing pebbles of the underlying granodiorite. On the east the formation is cut off by a steeply dipping fault, along which the basement rocks are intensely sheared and in places, finely ground to mylonite. There is a reversal of dip of the Catoctin Formation near this fault.
At least two minor faults cut the formation in this area. One extends from Hawksbill Gap down Cedar Run; the other goes through Franklin Cliffs (fig. 5) and down the valley of Rose River.
In the Big Meadows area, south of the Rose River, the Catoctin dips 10° to 15° S. Southwest of Big Meadows the greenstone crops out for several miles down Tanners Ridge. There the formation is exposed in a gentle anticline on the upper limb of the main Blue Ridge fold. Poor exposures and more intense sheering make it impossible to trace the flows in this area, but the anticline is indicated by the lower contact of the formation on the north slope of Tanners Ridge. The top of Chapman Mountain, just south of Tanners Ridge, is capped by several hundred feet of flat-lying lower Chilhowee sedimentary rocks on the crest of the subsidiary fold. These rocks are underlain by 50 to 150 feet of purple, red, or blue volcanic slate. The entire thickness of the greenstone in that area is only about 500 feet, as compared with greenstone at least 1,800 feet thick at Big Meadows, where the top of the formation has been removed.
Throughout the Big Meadows-Stony Man area cleavage strikes north of northeast and dips 30° to 60° E., except near faults. Lineation plunges east or southeast down the dip of the cleavage planes; it is marked by dark-green elongate chlorite blebs, faint striations on the cleavage, parallel orientation of actinolite needles in greenstone, and by elongated phyllite fragments in the sedimentary rocks.
The sedimentary rocks associated with the greenstones of the Catoctin Formation occur both at the base of the sequence and in thin interbeds between flows. Jonas and Stose (1939) described a sedimentary layer near the base of the greenstone near Swift Run Gap; they later named this layer the Swift Run Formation (Stose and Jonas, 1944). Bloomer and Bloomer (1947) recognized similar sedimentary rocks near Rockfish Gap and named them the Oronoco Formation. In the Big Meadows-Stony Man area a sedimentary layer occurs beneath the lowest flow, but because it is discontinuous and closely related to the sedimentary rocks interbedded with the overlying greenstones, it is not considered here as a separate formation.
Most of the basal sedimentary rocks of the Catoctin Formation are poorly sorted arkose, conglomerate, and graywacke. The graywacke contains angular to subrounded grains of glassy quartz and feldspar 0.1 to 3 millimeters in diameter in a grayish-green micaceous matrix composed of sericite and chlorite. This matrix material makes up 20 to 50 percent of the rock. Conglomerate composed of pebbles and cobbles of vein quartz and underlying gneisses in a matrix of graywacke is common. Pink, green, and gray phyllite fragments and small greenstone fragments occur locally. Detrital magnetite and hematite are common.
The arkosic sedimentary rocks are composed principally of angular to subrounded grains of clear quartz and white feldspar with a small amount of matrix material, mainly epidote; most arkoses are better sorted than the graywackes and many are crossbedded. Where the basal sedimentary rocks are thick they are generally graywackes or conglomerates; where they are thin they are arkoses or phyllites.
Near the head of Hawksbill Creek west of Big Meadows the basal Catoctin sedimentary rocks are about 100 feet thick and consist of graywacke and purple phyllite interbedded with finely laminated gray argillite. Each lamination in the argillite grades upward from the light-greenish-gray layer of coarse siltstone to a dark-gray argillite layer. The upper contact of the argillite layer is sharp and is overlain by the coarse silt layer of the next couplet of laminations. Thiesmeyer (1939) has described slates with similar laminations from Fauquier County, Va. He assigned them to the Loudoun Formation, apparently on the basis of Keith's geologic map of the Harpers Ferry quadrangle (Keith, 1894). A brief examination of the rocks at his locality, however, indicates that these slates are probably part of the basal Catoctin sedimentary rocks. Thiesmeyer gives an excellent description of the features and concludes that they are fresh-water varves, possibly of glacial origin. Although the general appearance of the laminations near Big Meadows and the gradation from coarse light-colored material at the bottom of each set to fine dark material at the top are very suggestive of glacial varves, no striated pebbles or rafted grains have been found associated with them. A glacial origin is, therefore, unproven.
At many places the lower contact of the basal sedimentary rocks is obscure. Graywackes with angular detrital grains grade downward into slightly sheared and altered gneiss. Some 50 to 100 feet below the sedimentary rocks the gneiss is fresh and contains large feldspar and quartz grains with little sericite. This effect may be due to weathering of the gneiss on the pre-Catoctin erosion surface, and much of the overlying sedimentary rock may be only slightly reworked from this weathered mantle.
The basal sedimentary layer of the formation has well-developed cleavage and lineation, marked by flattened and elongated phyllite fragments and parallel orientation of micaceous minerals. Quartz pebbles in the conglomerates are not visibly deformed, but their surfaces commonly have fine striations caused by flowage of the matrix that are parallel to the lineation of the enclosing rock. Banding in the granodiorite pebbles in the sedimentary rocks is not parallel to the cleavage of the enclosing rock.
The pre-Catoctin erosion surface has more than 1,000 feet of relief along the western boundary of the Catoctin outcrop area between Big Meadows and Stony Man. The thickest sections of the basal sedimentary rocks are near the low areas in the erosion surface. This indicates that the relief is not due to later deformation (fig. 4). In two places, streams have cut through Catoctin rocks and exposed hills of granitic rocks in the erosion surface which had been buried by the Catoctin lavas. The hill in Whiteoak Canyon had a relief of 450 feet, whereas the one in Hogcamp Branch was at least 750 feet high.
The sedimentary rocks between the lava flows are similar petrographically to the basal sedimentary rocks but are not extensive and are commonly only a few inches thick. Phyllites in the interbedded sedimentary rocks are common. They are generally gray but may be green, blue, or purple, and they contain few detrital grains. Phyllites of different colors are interbedded within a single outcrop, and they may show complex interfngering relationships. They are composed almost exclusively of sericite and probably were derived from alteration of volcanic ash layers.
In several places it has been possible to recognize and map individual flows within the greenstone sequence. At Franklin Cliffs at Crescent Rocks, on Stony Man, and in Whiteoak Canyon (fig. 6), massive greenstone layers form series of cliffs 150 feet high separated by talus-covered benches. Near the top of each cliff the greenstone is schistose (fig. 7), but a few feet down it is massive and irregularly joined. Locally, columnar jointing is well developed. Low-dipping joint sets similar to the flat primary joints in recent lava flows are commonly present, especially just below the schistose upper zone. The rock in the schistose layers is commonly a highly sheared breccia with fragments of amygdaloidal greenstone, silvery phyllite, and red argillite. The matrix is either epidote, greenstone, or phyllite. Locally, thin beds of sandstone occur in the sheared zones between the greenstone layers. The character of these breccias may not be apparent except on polished surfaces of hand specimens.
The sheared zones mark boundaries between lava flows and probably represent surface breccias, soil horizons, and thin sedimentary beds developed or deposited at the top of one flow before extrusion of the next flow. Loose blocks of lava and pieces of sedimentary rock torn up and churned into the base of the succeeding flow during its advance also make up part of the breccias. Deformation was concentrated at the flow boundaries, which left the greenstone near the centers intact and permitted preservation of primary features in many places.
In sections at Franklin Cliffs and at Crescent Rocks, both of which expose the lower three flows, all flows but one have a thickness of 150 to 200 feet (fig. 8). The second flow at Franklin Cliffs is about 270 feet thick. Northwest of Big Meadows, seven flows have a total stratigraphic thickness of 1,500 feet and an average thickness of 215 feet each.
It is generally difficult to trace an individual flow in the greenstone sequence because of the lack of continuous exposures, but the two porphyritic flows can be easily recognized and furnish excellent marker beds.
Because the pre-Catoctin erosion surface is irregular, the stratigraphic interval between the lowest of the porphyritic flows and the base of the Catoctin Formation varies. On Hawksbill Mountain the lowest porphyritic flow is the sixth flow above the base of the formation. North of Big Meadows it is the fourth, and west of Big Meadows it is the second or third flow above the base. At the head of the Rose River the lowest porphyritic flow probably abuts against the granodiorite hill exposed in the canyon of Hogcamp Branch.
The flows below the lowermost porphyritic flow are the best exposed in the volcanic sequence. The greenstone of these flows is fine grained and generally nonporphyritic, although sparse small plagioclase phenocrysts are present locally. Interbedded phyllitic sedimentary rocks are common, and columnar jointing is well developed in one flow and distinguishable in several others. Flow boundaries exposed in the cliffs are marked by intensely sheared zones of volcanic breccia. Most of the primary features described below are best observed in this group of flows.
The greenstone of the lower porphyritic flow has a medium- or coarse-grained groundmass with plagioclase crystals about 1 millimeter long. The plagioclase phenocrysts (now albite) are 5 millimeters to 1.5 centimeters long and make up 15 to 30 percent of the rock. The flow has been traced for more than 6 miles, though its position is indefinite in areas where outcrops are poor or where intense shearing has obscured the porphyritic character. The flow commonly forms cliffs, even where exposures of the other flows are poor. On Tanners Ridge southwest of Hawksbill Creek, the flow could not be traced because of poor outcrops and intense shearing. The porphyritic character becomes less distinct to the north near Stony Man. The flow must have covered an area of at least 15 square miles.
The upper porphyritic flow, 400 to 800 feet stratigraphically above the lower porphyritic flow, cannot be traced over as large an area as the lower flow. The upper flow closely resembles the lower flow in most outcrops, but in places it contains large phenocrystssome are as much as several centimeters longthat make up as much as 50 percent of the rock. Three to five flows may be present between the two porphyritic flows, and sedimentary interbeds are sparse.
The flows above the upper porphyritic flow are poorly exposed, and the maximum number still preserved is undetermined. Much of this sequence consists of fine-grained nonporphyritic greenstone, but coarse-grained types with scattered phenocrysts are common. A few sedimentary interbeds less than a foot thick occur. Approximately 700 feet of greenstone is preserved above the upper porphyritic flow on the slopes south of Spitler Hill. The Catoctin is at least 1,800 feet thick in this area, and the top has been removed by erosion. This may be the maximum thickness preserved in the Big Meadows-Stony Man area.
The preservation in the greenstone of some of the typical primary structures of more recent basalt flows is of interest because these structures afford important clues to the origin of the greenstone and because their preservation indicates the small amount of deformation that some of the rocks have undergone.
A flow with unusually well-developed columnar jointing can be traced discontinuously near the bottom of the greenstone sequence from Big Meadows to Stony Man. The columns are approximately a foot in diameter and as much as 20 feet long (fig. 9, top photo). The faces of the columns are commonly marked by faint grooves normal to the axes. Most of the columns are broken along cleavage planes (fig. 9, bottom photo). In most exposures of this flow the axes of the individual columns are parallel, but in a few places, for example at Crescent Rocks, the axes are curved and randomly oriented.
Many flows show rude columnar jointing; generally the columns are 2 or 3 feet in diameter and considerably shorter than those in the flow just described. Some flows have large columns near the base and smaller ones near the top.
The columns have been deformed so that their axes are no longer perpendicular to the surfaces of the flows, but plunge to the south or southeast at angles of as much as 50° with the normals to the flow surface.
Low-dipping primary joints
Many greenstone exposures have a prominent low-dipping joint set, which gives the outcrops a steplike appearance. The joints are related to flow surfaces, and they may be used in the field to determine the approximate attitude of the flows. The joints are probably analogous to the original joints parallel to flow surfaces, which are common in recent basalt flows. The joints are spaced a few inches to several feet apart and are more pronounced near the top of a flow. Farther down in a flow they are generally absent.
Amygdules, or filled gas bubbles, occur in almost every greenstone outcrop and are especially abundant in zones near flow tops. The characteristic minerals in the amygdule fillings are milky quartz, epidote, albite, calcite, and chlorite (fig. 10). An amygdule may be filled with a single mineral or with several minerals in concentric layers or irregular intergrowth. Epidote, quartz, and albite are commonly associated, in the amygdule fillings. Chlorite and albite are common associates, albite forming the rim and chlorite forming the core of the amygdule. Chlorite occurs alone in some amygdules.
In thin section (fig. 10, photomicrograph), the chlorite filling commonly shows an outer layer composed of a fibrous aggregate of chlorite in which the long axes of the fibers are perpendicular to the wails of the amygdule. The core is composed of an aggregate of chlorite of the same color.
Amygdules in the greenstone are generally almond shaped where scattered, but in the highly amygdaloidal zones they are irregular in outline. Some of the larger amygdules have rounded upper surfaces and flat bottoms parallel to the flat primary jointing. In some places the amygdules are arranged in layers which are probably related to flow planes in the lava.
Interbedded sedimentary members of the Catoctin Formation commonly show complex and confusing relations to the greenstone. Near the top of a flow, sedimentary rocks from an overlying lens may extend downward along cracks 5 or 10 feet into the greenstone. These sedimentary dikes are as much as 3 inches wide and contain sediments similar to those immediately overlying the flow. They probably represent sand and mud that sifted down into cracks soon after the molten rock solidified.
Sedimentary dikes of a different type occur near the bases of some of the flows (fig. 11), where sedimentary rocks project upward into the greenstone in a network of branching veins. These veins extend 10 or 15 feet above the bases of the flows, beyond which they gradually die out in solid greenstone. These dikes were probably formed as a result of the advance of a lava flow over wet sediments. Steam pressure and the weight of the overlying lava forced the soft, unconsolidated sediments up into cracks in the abruptly chilled lava at the base of the flow, and formed a network of sedimentary dikes. On polished surfaces the greenstone is dark green and very fine grained for a few millimeters away from the contact with the sedimentary rocks, whereas farther away it is greenish gray and coarser grained. The dark fine-grained border probably represents a thin selvage of glass that formed when the lava came in contact with the wet sediments, but the glass has been altered to a dense, fine-grained aggregate consisting mostly of chlorite.
Flow boundaries are generally marked by zones of breccia as much as 20 feet thick containing fragments of amygdaloidal greenstone, purple phyllite, and red or pink sandy argillite. Angular fragments of specular hematite are common in some of the breccias. The most common types of breccia are epidoteamygdaloid breccia and mud-lump breccia. The epidote-amygdaloid breccia (fig. 12) is composed of angular or irregular rounded fragments of purple, red, or blue-gray amygdaloidal greenstone set in a matrix of fine-grained greenstone, quartz, and epidote. The amygdules are filled with milky quartz and epidote. Fragments range from 2 inches to several feet across. This breccia probably represents a frothy crust that formed on the lava flow and was broken up by further movement of the still-liquid lava beneath. Because of easy access along these zones, hydrothermal solutions, have almost completely replaced the breccias with epidote and quartz.
The mud-lump breccias consist of angular or subangular fragments of pink or reddish-brown sandy argillite or sandstone in a matrix of fine-grained schistose greenstone or silvery phyllite, and they contain only minor amounts of epidote (fig. 13). On slightly weathered surfaces the mud lumps stand out in relief. Most are dense very fine grained pink or red rocks whose sedimentary character is not apparent except where thin sandy stringers are present or where there is a gradation from sandstone into red argillite containing scattered sand grains. The mud lumps may be pieces of a thin soil mantle or sedimentary layer formed on top of one flow and later churned into the base of the next flow. The red mud which formed the bulk of the sedimentary material probably was derived from weathering of underlying lava; the sand grains, mostly quartz, must have come from an outside source, probably some nearby granitic hill still unburied by lava. The silvery phyllite may represent tuffaceous material. In a few places thin layers of material similar to the mud lumps are found undisturbed between flows, possibly indicating old soil horizons.
Feldspar laths, chlorite, and epidote are seen with a hand lens in coarse greenstone, but in the fine-grained greenstone none of the rock minerals can be identified without a microscope. Native copper occurs in minute flakes at a few localities.
Some flows contain scattered phenocrysts of plagioclase, but phenocrysts are rare at most localities. The two porphyritic flows contain plagioclase phenocrysts as much as 1 centimeter long (fig. 14); the phenocrysts make up as much as 30 percent of the rock. On freshly broken surfaces the phenocrysts may be obscure, but they weather bone white and are conspicuous on slightly weathered surfaces. The unusual porphyritic texture of these flows has made it possible to distinguish them from the other flows in the lava sequence and to trace them for considerable distances.
The greenstone is commonly cut by veinlets of quartz and epidote which are also the typical minerals in the amygdule fillings. In many places the greenstone has been completely replaced by epidote and quartz and forms a hard yellowish-green rock. The epidote-quartz rock is characteristically cut by narrow, nearly horizontal gash fractures containing quartz and fibrous anthophyllite. The veins are generally only a few millimeters thick, but are as much as several centimeters thick at a few localities.
The epidote-quartz rock occurs in large pods and irregular masses associated with epidote-quartz veinlets. The contact of these masses with the normal greenstone may be sharp, in which case it is usually a joint plane, or is gradational for several inches. Where this type of alteration has occurred, amygdules and plagioclase phenocrysts have been replaced by quartz.
Minor amounts of native copper are found in the greenstones of the Catoctin Formation, and unsuccessful attempts at copper mining were made at several localities. Two prospects within the area were worked in 1854-56 and are described briefly by Weed and Watson (1906). One of these, just north of the summit of Stony Man, was opened by a shaft of unknown depth which has now been filled. The other prospect is on the ridge north of the confluence of the Rose River and Hogcamp Branch in the zone of northwest-trending cleavage which is believed to mark the Rose River cross fault. Its workings comprise a few shallow prospect trenches and a shaft that is flooded to the surface. Judging from the size of the dump, the prospect is only a few feet deep.
In thin section, the chief minerals of the normal greenstone are seen to be chlorite, actinolite, epidote, albite, magnetite, specular hematite, sphene, and pyroxene. Small amounts of quartz and calcite are also common. Only the pyroxene and part of the magnetite are believed to be primary minerals of the original lava.
Where the greenstones are not sheared the texture is that of the original lava (fig. 10, photomicrograph). The rock consists of interlocking plagioclase laths (now albite) in an interstitial mat of chlorite, actinolite, epidote, sphene, leucoxene, and magnetite. Original pyroxene grains are common between the laths in some specimens, but in most of the finer grained rocks the pyroxene is almost completely altered. This texture suggests the typical basaltic textures in which the spaces between the plagioclase are filled with either granular crystals of pyroxene or basalt glass. Large irregular patches of chlorite are fairly common in the greenstone.
In the sheared or more schistose greenstone the original texture has been destroyed, and the rock consists of actinolite needles and equidimensional grains of epidote, sphene, and opaque minerals set in a chloritic matrix. Small irregular grains of plagioclase are generally present.
Where the greenstone is completely replaced by epidote and quartz, these secondary minerals form equal-sized grains. Under the microscope, the basaltic fabric may still be seen and is almost perfectly preserved. Feldspar laths are entirely replaced by fine-grained aggregates of quartz, and the interstitial minerals are replaced by epidote and quartz. Outlines of amygdules are preserved, but their fillings have been replaced by mosaics of fine-grained quartz.
The granitic rocks underlying the Catoctin Formation are cut by dikes of greenstone ranging from a foot to 50 feet or more in thickness. Most of the dike rocks are fine grained and resemble the greenstones in the flows. Many dikes have columnar joints normal to the walls; some have a faint cleavage parallel to that in the rocks overlying the granitic basement. Most dikes have a thin fine-grained margin, probably caused by chilling against the walls. Several dikes on Old Rag Mountain contain crystals of plagioclase as much as 1 centimeter across.
Good examples of these dikes are found along the Skyline Drive in the roadcut north of Shavers Hollow parking area where at least six crop out within a distance of 1,500 feet.
Several large dikes, one of them 50 feet thick, and many smaller ones cut through the granite near the summit of Old Rag Mountain; they are less resistant to erosion than the granite and form deep notches in the summit ridge (fig. 15, top photo). A dike 15 feet thick with columnar jointing is exposed at the north end of the tunnel on Skyline Drive about three quarters of a mile south of Thornton Gap (fig. 15, bottom photo). The attitude of the dikes is generally difficult to determine precisely, but most strike north and dip between 65° E. and 65° W.
The greenstone in the dikes is composed of pyroxene and plagioclase in a mat of secondary chlorite and minor amounts of calcite, quartz, and epidote. Chlorite replaces plagioclase in many places and isolated rounded grains of pyroxene are left in a chloritic mat.
In most places the Catoctin Formation and the overlying Chilhowee sedimentary rocks are separated by a thin layer of purple, reddish- or chocolate-brown volcanic slate which is spotted with tiny white circles or ovals and which has been described by Furcron and Woodward (1936) as a basal Cambrian lava flow. King (1950) mapped the slate in the Elkton area as the Loudoun Formation and considered it to be composed of detrital materials that were explosively ejected from a volcanic vent. This rock underlies the Chilhowee sedimentary rocks that cap Chapman Mountain; it crops out in a narrow belt west of Lucas Gap on Tanners Ridge and crops out discontinuously along the upper contact of the Catoctin at least as far north as Knob Mountain, north of Jeremys Run. The slate averages 50 to 100 feet in thickness but locally reaches 200 feet. North of Beahms Gap it is absent in several places, and the lower beds of the Chilhowee Group rest directly on greenstone of the Catoctin Formation. Furcron and Woodward (1936) state that the slate "has been found * * * above granodiorite in the absence of any greenstonea fact that strongly suggests that the extrusive [slate] is later or younger than either the greenstone or granodiorite."
Under the microscope the rock commonly shows rectangular laths, probably representing original plagioclase that is now completely replaced by sericite, in a matrix of sericite and dark opaque material. Scattered throughout the rock are green chlorite clots, and small wedge-shaped crystals of sphene are common. A few unaltered remnants of pigeonite occur. The spots, which range from 1 to 2 millimeters in diameter and appear white in the hand specimen, are dark and nearly opaque in thin section. They are oval in general plan, but in detail their boundaries are highly irregular and spongelike. They include sericitized plagioclase laths, some of which extend across the boundaries of the spots. Where shearing has destroyed or modified the fabric of the rock as a whole, the replaced plagioclase laths within the spots preserve a basaltic texture.
Field relationships and petrography suggest that the slate is a metamorphosed saprolite (weathered residual rock) developed at the top of the Catoctin Formation before deposition of the overlying sediments. Where the weathered material was reworked during deposition of the basal bed of the Chilhowee, the volcanic texture was lost, but where the saprolite was not disturbed the texture is locally preserved.
Thin layers of similar slate and purple argillite lie between flows in the greenstone of the Catoctin, and veinlets of jasper with detrital sand grains penetrate the greenstone near the tops of some flows. Weathering of basalts commonly leads to the formation of similar jasper veinlets. King (1950) reports jasper masses in the slate in the Elkton area.
That the slate immediately overlies the granitic rocks in a few places may merely indicate that a thin Catoctin flow was completely weathered in place before deposition of the Chilhowee beds.
The volcanic nature of the greenstones of the Catoctin Formation has long been recognized, but little has been published concerning the original composition of the Catoctin lavas and their mode of eruption. Most authors agree that the bulk of the lavas were basalts, although Bloomer and Bloomer (1947) concluded that the lavas were andesites on the basis of the composition of the plagioclase, which they reported as being andesine. Determinations by the writer, however, indicate that the plagioclase is albite. Conclusions about the original character of the Catoctin lavas, however, cannot reasonably be based on the present composition of the plagioclase. Relic textures strongly indicate that the lavas were basalts, and this conclusion is supported by the mineralogy of the rocks and by the available chemical analyses (Reed, 1964).
The Catoctin lavas probably were plateau basalts erupted from fissures in the basement rocks. The thickness and extent of the flows, absence of known central volcanoes, and flood-like character agree with the characteristics of plateau basalt accumulations.
The association of the greenstone of the Catoctin with the sedimentary rocks of the Appalachian geosyncline brings up the question of its relationship to albite-bearing (spilitic) lavas so characteristic of the early stages of many geosynclines. Although the origin of the albite in basalt has been much debated, many recent authors agree that it is secondary because partially replaced labradorite cores are common in some of the albite crystals and because albite and pyroxene would probably not crystallize simultaneously from a magma (Gilluly, 1935).
The greenstone of the Catoctin is similar to some spilites in certain respects, but it differs from them in other important features. First, the Catoctin flows were clearly erupted on land as is shown by the presence of columnar jointing, absence of pillow structure, areal extent of individual flows, and relatively thin breccia zones between flows, while spilites are typically erupted under water and show well-developed pillow structure. Second, spilities are characteristically associated with great thicknesses of graywackes and bedded cherts containing occasional limestone lenses, whereas the sedimentary members of the Catoctin Formation are insignificant and are arkoses derived from local sources in the nearby granitic rocks. Third, there is no evidence that the albite and other secondary minerals were formed during or immediately following consolidation of the flows. Alteration did not occur until after soil zones had formed and the overlying sedimentary rocks were deposited. For these reasons the mineralogy of the Catoctin greenstone can best be explained as the result of low-grade regional metamorphism of an accumulation of plateau basalts without important change in the bulk composition (Reed, 1964).
Last Updated: 28-Jan-2007