B3: EXAMPLES OF ALONG-STRIKE CHANGES IN FOLD-THRUST BELT ARCHITECTURE; STRUCTURAL GEOLOGY OF THE ROSENDALE NATURAL CEMENT REGION, ULSTER COUNTY, NEW YORK
Kurtis C. Burmeister and Stephen Marshak
Department of Geology
University of Illinois
Urbana, Illinois 61801
INTRODUCTION
It was necessary for the leaders of this trip to specify a set number of vehicles to obtain permission to visit several of the following stops. For this reason, personal cars will not be allowed to follow the field trip caravan. Throughout much of the 19th century, the Rosendale natural cement region (Figure 1) was recognized worldwide as a center for the production of high-quality hydraulic cement. Although the industry collapsed in the early 1900s, the geology of this region continues to attract attention. The Rosendale area contains the northernmost portion of the central Appalachian foreland fold-thrust belt. This fold-thrust belt segment lies in the southern arm of the New York recess, a convex to the foreland, map-view curvature in the Appalachian orogen. Fold-thrust belt deformation across the New York recess involves a mechanically rigid strut of Late Silurian through Middle Devonian sedimentary strata (Figure 1; Wanless, 1921; Waines and Hoar, 1967; Rodgers, 1971; Marshak, 1986; Epstein and Lyttle, 1987; Marshak and Tabor, 1989; Marshak, 1990). This rigid strut is sandwiched between thick, relatively ductile units of Ordovician shale (below) and Middle Devonian shale (above). Near Rosendale, the Siluro-Devonian strut thins markedly from greater than 1000 m thick in central Pennsylvania to little more than 100 m thick north of Kingston. These contrasts in the pre-deformational stratigraphy of the affected units give rise to dramatic, along-strike transitions in the scale, style, and trend of structures in the fold-thrust belt across the New York recess. Preliminary balanced cross sections based on recent geologic mapping in the vicinity of Rosendale, combined with recently re-discovered historical photographs, are providing new insights into the structural relationships underlying these along-strike transitions in fold-thrust belt architecture. Specifically, the south to north thinning of the Siluro-Devonian rigid strut that takes place near Rosendale appears to trigger a south to north: 1) slight westward rotation of structural trends in the fold-thrust belt; 2) eastward migration of the pin line of deformation resulting in a narrower cross-strike fold-thrust belt width; 3) tightening of fold amplitudes and wavelengths; 4) decrease in the spacing between thrust faults and the development of lateral ramps; 5) northward dying out of thrust faults into fault-propagation folds, and 6) redistribution of regional detachment horizons.
The Rosendale natural cement region is ideally suited for the study of along-strike changes in the architecture of fold-thrust belts. In particular, the unique regional stratigraphy provides a basis for directly examining the role of changing mechanical stratigraphy in the development of along-strike changes in the internal architecture of these tectonic provinces. Further, the fold-thrust belt near Rosendale contains all of the structural complexities of regions like the Valley and Ridge Province ofPennsylvania, yet with a cross-strike width of little more than 2 to 8 km, it is possible to walk transects of the fold-thrust belt in one day. This excursion will focus on the following aspects of the Rosendale region's geology. The Rosendale region is an ideal place to examine: 1) fault mechanisms, including ramp-flat thrust fault geometries, accommodation faulting, and duplex structures; 2) fault-bend, fault-propagation, and detachment folding; 3) strain distribution in thrust sheets; and 4) the controls of rock type and structural relationships on cleavage morphology and intensity. In addition to structural relationships, the strata in the Rosendale region preserve an abundance of Early to Middle Devonian marine fossils, so we can examine examples of classic shallow-marine carbonate facies successions (Rickard, 1962; LaPorte, 1969), and outcrops of the region provide exposures of the Taconic angular unconformity (Rodgers, 1971; Toots, 1976; Epstein and Lyttle, 1987).

B3: EXAMPLES OF ALONG-STRIKE CHANGES IN FOLD-THRUST BELT ARCHITECTURE; STRUCTURAL GEOLOGY OF THE ROSENDALE NATURAL CEMENT REGION, ULSTER COUNTY, NEW YORK

Shallowly west-dipping beds of the Union Springs Formation
Road cut exposures of shallowly west-dipping beds of the Union Springs Formation along the left (northwest) side of Route 209 North

Bridge crossing Esopus Creek

Broad, open anticline in Schoharie Formation and Onondaga Limestone.

STOP 1. Folds exposed in road cuts along State Route 209 north of Kingston
During our drive east, we have passed from the foreland of the Appalachian orogen into the core of the Hudson Valley fold-thrust belt north of Kingston. Here, road cuts along State Route 209 expose large, slightly asymmetric open folds with no visible thrust faulting or mesoscopic folding. The geology of this stop was first described by McEachran (1985) and later used as a field trip stop by Marshak (1990). Five major, map-scale fold hinges cross State Route 209 between Routes 9W and 32. The most prominent of the folds at this stop is a large anticline (Figure 3) involving the upper Becraft Limestone, the Alsen Formation, and the Port Ewen Formation. Note the differential development of cleavage in these units. The Becraft Limestone contains little to no cleavage, while the Alsen and Port Ewen Formations clearly possess a strong, southeast-dipping cleavage. Marshak (1990) notes that these folds are characteristic of structural styles north of Kingston, in that they trend roughly 015° and lack structural complexity. Return to the vehicles and carefully merge back into traffic. As we proceed a short distance further to the east on State Route 209, notice the west-dipping beds of the Manlius through New Scotland Formations.

STOP 2. Laterally ramping thrust faults in road cut along Route 32 north of Kingston
Four major thrust faults duplicate the Rondout and Manlius Formations in a series of imbricate thrust sheets in the northern half of the long road cut along the west side of State Route 32 (Figure 4). The geology of this stop was first described in detail by Waines and Hoar (1967) and was further interpreted by McEachran (1985) and Marshak (1990). The major thrust faults in this outcrop strike roughly 040° and calcite slip fibers on these faults suggest a transport direction of 060°-070°. In places, these faults have a flat-on-flat geometry (i.e. the thrust faults are parallel bedding in both the hanging wall and footwall), suggesting large displacements. In places (particularly in the upper portion of fault block 6; Figure 4), thrust faults appear to cut down section. However, this is likely an artifact of the obliquity of the road cut face to the structures, where the hanging walls are thrust westward into the outcrop. These faults could not be traced west of the road cut, but may ramp laterally up-section and die out to the north. Return to vehicle and continue south on State Route 32 South. From here, we will proceed southeast towards the Helderberg

STOP 3. Complex structural relationships of Hasbrouck Park, east Kingston
Lock cars and follow the footpath at the east end of the parking lot for roughly 75 m as it descends around the nose of a small hill of Manlius, Coeymans and Kalkberg Formations south of the trail. At the foot of this slope is an abandoned adit cut into an extensively quarried face in the Helderberg Escarpment. The geology of the Helderberg Escarpment at Hasbrouck Park was fist described by Marshak and Tabor (1989; Figure 5) and later revisited as a field trip stop by Marshak (1990). This face provides a cross-sectional view through the leading edge of a duplex composed of a stack of horses involving Rondout through Kalkberg Formation strata (Figure 5B). The basal thrust fault in this duplex, the Hasbrouck thrust, cuts laterally up section along the sloping footpath we walked along (Figure 5C), and through the woods. The Hasbrouck thrust fault reappears on the north side of Delaware Avenue, where it places the Manlius Formation over the Alsen Formation, above extensive roof-and-pillar cement mines just east of Corporate Drive. A tear fault with a trace roughly coincident with Delaware Avenue may extend to the west of the lateral ramp. The complexity of these structural relationships amongst the Silurian and Devonian strata in Hasbrouck Park is characteristic of the geology along the Helderberg Escarpment at the latitude of Kingston.
Return to main footpath and follow it further to the south, skirting along the base of the Helderberg Escarpment. Stay to the right at the first fork in the footpath and proceed up narrow ridge. From this locality, it is possible to observe steeply dipping to overturned beds exposed by quarrying of portions of the Rondout Formation. Retrace your path along the ridge back to the main footpath, return to the vehicles, and exit the park. We will now proceed south and examine some of the along-strike changes in structural architecture of the eastern margin of the northern Appalachian fold-thrust belt near Rosendale.

Note entrances to the abandoned Delaware Mine
Note entrances to the abandoned Delaware Mine on left (west) side of road. This mine was most recently used by the Knaust Brothers to grow 'Fallout Proof mushrooms during the 1950s.

Note abandoned canal barge in tidal flats off to left (east).

The Mansion House located on this corner
The Mansion House located on this corner was built in 1833 by Jervis McEntee, one of the engineers that pointed to Rosendale as a local source for hydraulic cement for construction of Delaware & Hudson Canal (Werner, personal communication, 2003).

Note various ruins of cement kilns and associated buildings along next the road over the next kilometer.

This road follows the path of what was originally a plank road
This road follows the path of what was originally a plank road and later the roadbed of the horse-drawn Hickory Bush-Eddyville railroad. A consortium of cement companies constructed and maintained this throughway to avoid the shipping fees charged by the Delaware & Hudson Canal for moving their product from Hickory Bush to Kingston (Werner, personal communication, 2003).

Abandoned roadbed for Hickory Bush-Eddyville railroad
Abandoned roadbed for Hickory Bush-Eddyville railroad diverges from course of DeWittLake Road and is visible in trees off to right (west)

STOP 4. North end of Quarry Hill, Bloomington
This stop is on private property. You must obtain permission to visit from the owners of the house near the garage before proceeding. Walk the short distance to the garage on the edge of the tree line just south of the parking lot. Upon reaching the tree line, you will notice two depressions just through the trees to the south. These are the northern end of a series of extensive abandoned cement quarries spanning the entire length of Quarry Hill. Please proceed with caution.
First, walk into the western quarry pit. Here, a small quarry exposes east-dipping strata of the Rosendale and Glasco Members of the Rondout Formation. Retrace your path back to the edge of the tree line, and circle back around to the eastern quarry opening. Watch your step as you descend into this quarry. The slope is uneven and littered with broken glass and scrap metal. Here, the Rosendale Member of the Rondout Formation was extensively mined (all that remain are support pillars) and affords a fantastic view to the south along the axis and steeply dipping eastern limb of a northwest-verging syncline (Figure 6). The eastern quarry wall contains the gradational contact between the Rosendale Member and the underlying Binnewater Sandstone. The base of the Glasco Member forms the western quarry wall.
Note the tight hinge of the syncline and recall the relationship observed in the smaller quarry to the west. A northwest dipping, out-of-the-syncline thrust fault that apparently ramps up section out of the Rondout Formation separates the two quarries at this location (Figure 7). Thus, strata exposed in the western quarry are in the hanging wall, and were thrust to the southeast over the strata in the eastern quarry. Consider the contrasts in structural style between this location and the complex duplexes and the stacking of imbricate thrust sheets near Kingston. The quarry exposures at this location afford an excellent view of the structural relationships that are characteristic along the Helderberg Escarpment between Bloomington and Rosendale. Here, the escarpment is defined by a series of left-stepping, thrust faults that cut up section to the east, out of the cores of large synclines.

STOP A. Road cut exposure of folds along Route 32, north of Rosendale
The road cut along the west side of State Route 32 at this locality exposes a tight, northwest verging anticline in the Kalkberg Formations. This structure is a continuation of the same series of folds exposed in the mines along Quarry Hill (Figure 7). The dip of the strata in the western limb of this fold continues to increase westward. Exposures of Becraft through Port Ewen Formations are steeply dipping to overturned in road cuts along the New York State Thruway.

STOP B. South end of Quarry Hill, Bloomington
This stop is on private property and permission to visit must be obtained in advance. Trespassers will be prosecuted.
Walk north along the small dirt road located across from the house, keeping to the right as the road descends into the mouth of an abandoned cement quarry. The quarry at this locality is the southernmost of the Quarry Hill mines. Both the Rosendale and Whiteport Members of the Rondout Formation are extensively quarried at this location (Figure 15). Steeply dipping beds of the base of the Rosendale Member and the Binnewater sandstone form the eastern quarry wall. Moderately dipping beds of the Rondout through Manlius Formations form the western quarry face. The large, central quarry area exposes strata of the Rosendale Member that are repeated by two major thrust faults and extensively cut by a number of smaller thrusts. The easternmost of the two major thrust faults is steeply west dipping and exhibits a hanging wall ramp on footwall flat geometry. The western major thrust fault is moderately west dipping and also has a hanging wall ramp on footwall flat geometry. The western fault contains a horse of Rosendale Member. The two major thrust faults merge near the top of the quarry. The hanging wall of these faults is involved in a northwest-verging syncline, but is apparently not faulted. Some amount of bedding-parallel slip has also occurred along the eastern quarry wall. A close examination of this surface reveals a well-developed set of non-coaxial slip fibers. The faults exposed at this location are not continuous with those exposed at the north end of Quarry Hill (Stop 4).

Well-preserved cement kilns on left-hand (northwest) side of road

Entrance to the mines on right-hand side of road
Entrance to the mines on right-hand side of road were once operated by the Lawrence Cement Company (Werner, personal communication, 2003), and are presently owed by Iron Mountain Incorporated as a future archival site.

Cement kiln ruins on right-hand (southeast) side of road

STOP 5.1. Eastern limb of the Hickory Bush anticline, Rosendale Landfill
Lock vehicles and walk approximately 100 m northeast along Hickory Bush Road to the entrance of the Rosendale Landfill and Recycling Center. Proceed through gate and to the north corner of the facility. Recent excavation along the north wall created fresh exposures of an east-dipping sequence of strata (Figure 8). The north wall of the landfill contains Martinsburg Shale, the Taconic unconformity, Shawangunk Conglomerate, High Falls Shale, Binnewater Sandstone, Rondout Formation, and Manlius Limestone.
From a distance, the Martinsburg Shale appears un-deformed, but closer examination reveals that it is strongly deformed by complex brittle faulting. Above the Taconic unconformity, the Shawangunk Conglomerate is little more than a 5 to 10 cm thick lag deposit of the characteristic milky white quarts pebbles. Overlying the Shawangunk Conglomerate is a complete and apparently continuous sequence of High Falls Shale and Binnewater Sandstone. Both the Rosendale and Whiteport members of the Rondout Formation are quarried at this location. Separating the two quarries is the Glasco Member, which contains beautiful Halycities chain corals. At the eastern end of the north wall are exposures of the overlying Manlius Limestone, which are in faulted contact.
The east-dipping strata exposed in the Rosendale Landfill form the eastern limb of the Hickory Bush anticline. The involvement of Martinsburg Shale in core of the fold suggests this structure developed as the result of slip along a detachment at depth in the underlying Ordovician strata. The large scale of the Hickory Bush anticline suggests that the underlying thrust is a master fault in the fold-thrust belt at this latitude and ramps directly from the lower detachment horizon. The thrust fault exposed at the eastern end of the exposures along the north wall is the westernmost fault in a complex imbricate fan of thrusts that ramp out of the Rondout Formation and cut through Hickory Bush Hill (the large hill southeast of the landfill).

STOP 5.2. Western limb of the Hickory Bush anticline, rail cut near Fourth Lake
Walk southwest along the rail trail from the parking lot along Hickory Bush Road for roughly 350 m until you encounter a rail cut exposing moderately northwest dipping strata on both sides of the trail. The exposed sequence includes High Falls, Binnewater, Rondout, and Manlius Formations (Figure 9). Along the northwest side of the trail, the High Falls Shale is difficult to distinguish, but it is overlain by a complete thickness of the Binnewater Sandstone. Cross bedding, ripple marks, and graded bedding are clearly visible, as is a characteristic, roughly 10 cm thick shale horizon just below the contact with the overlying Rondout Formation. This shale layer is also present in an outcrop of the Binnewater sandstone at the Snyder Estate, where it is deformed. The Rosendale and Whiteport members of the Rondout Formation are quarried at this location. Notice how air circulating through the abandoned mines keeps this area noticeably cooler during the hot summer months.
Climb onto the embankment on the south side of the rail trail using the small path through the trees located just north of the northernmost quarry opening. The embankment was once a tramway that serviced the cement quarries in this area. Watch your step. Abandoned cement kilns and sunken shed foundations are scattered along this tramway and are often difficult to see. Proceed along tramway to the southeast, skirting along an exposure of the Binnewater Sandstone. When the tramway narrows and prevents further progress, drop down the slope to the next lower abandoned roadbed and continue to the southeast. After hiking approximately 150 m from the rail trail, you will reach and intersection with a dirt road. This road is part of the Perfume Trail on the Williams Lake Resort. Follow the dirt road to the right (southwest) and you will soon see a large mine entrance. Proceed about 10m into the mine.
This mine was operated by the Lawrence Cement Company (Werner, personal communication, 2003) and is cut into the Rosendale Member of the Rondout Formation. The contact with the underlying Binnewater Sandstone forms the floor of the mine, and the contact with the overlying Glasco Member forms the ceiling (Figure 10). The quarry is in a large, asymmetric, open anticline. Note how the shallow dip of strata in the western limb of the fold gently increases to the southwest. Proceed southwest into the mine along the axis of the fold. Note the relatively rapidly increasing dip of the strata in the eastern limb of the fold. Quarrying of the eastern limb was most likely halted due to the proximity of a fault with a trace that roughly follows the path of the Perfume Trail a few meters further to the east.
Climb up and out of the mine through the opening left by the partial collapse of the roof at the southeast end of the quarry. As you climb out of the mine, pause to note the other portions of the quarried fold around the periphery of the collapsed area. It is unclear whether strata of the Whiteport Member above the quarried fold was removed by erosion or was stripped by quarrying. Follow the footpath path down to the Perfume Trail and continue to the south until you reach a intersection of several trails. Return to the vehicles by walking north along the rail trail (covered in black gravel) from this junction. Along the way, note the various quarries and outcrops as you pass through the Fourth Lake region. The Williams Lake Resort property around Fourth Lake contains some of the best exposures of structural relationships in the region, and has long been used to teach the methods of field geology.

Binnewater Road follows the trace of the axis of the Binnewater anticline.

The south quarries of the F.O. Norton Company
The south quarries of the F.O. Norton Company in east-dipping units of the Rondout Formation located in the escarpment through trees on left (east) side of road.

The Beach Mine of the Lawrenceville Cement Company
The Beach Mine of the Lawrenceville Cement Company (Werner, personal communication, 2003) in west-dipping strata of the Rondout Formation along right (west) side of road. Iron Mountain Incorporated now uses these mines as a document storage facility.

The Hoffman Quarry of the Lawrence Cement Company
The Hoffman Quarry of the Lawrence Cement Company located east of small Wallkill Valley RR trestle on left (east) side of road. A battery of abandoned cement kilns built by the Lawrenceville Cement Company is visible on the right (west) side of road (Werner, personal communication, 2003).

Stone reservoir along right (west) side of road.
This pond was created in the late 1820's to ensure a constant reserve supply of water for a feeder stream that was used to replenish water levels in the Delaware & Hudson Canal (Werner, personal communication, 2003).

Joppenbergh Hill
Joppenbergh Hill is located immediately to the left (east) of this intersection. The hill is named after Jacob Rutsen, who became the first westerner to settle in the Rosendale vicinity in 1680. The New York and Rosendale Cement Company extensively mined Joppenbergh Hill during the 1800's. Large sections of the resulting quarry faces began collapsing in 1899, and have continued to do so as recently as April 2003. Rosendale Bridge, built by the Wallkill Valley Railroad, spans Rondout Creek from the flank of Joppenbergh Hill. Locally, State Route 213 follows the northern bank of Rondout Creek, and coincides with the trace of the Delaware & Hudson Canal. A thick, east-dipping sequence of Shawangunk Conglomerate cropping out in the south banks of the creek is visible through the trees.

OPTIONAL STOP C: Butler's Lock Quarry
This is private property and permission must be secured in advance to park in this lot. Many aspects of this stop are extremely dangerous and should only be attempted by very small groups. Pull off State Route 213 into the parking lot of the Butler's Lock Quarry and the Turco Brothers Water Service, and park out of the way. Beware that semi trucks hauling full-sized water tanks enter this lot at full speed and use portions of this space to turn around. Care must be taken when parking and walking about the lot.
Century thrust fault, road cut along State Route 213 east of Rosendale Portions of this stop are on private property and permission to visit must be obtained in advance. Trespassers will be prosecuted.
Park vehicles out of the way of traffic in the lot and walk westward along the north side of State Route 213, keeping the guardrail between you and the traffic. The large quarried face to the north is the Butler's lock Quarry and includes a continuous sequence of Rondout though Kalkberg Formations. As you proceed along the road, note how the strata in the Butler's lock Quarry are folded into a small syncline. Once at the western end of the guardrail, very carefully cross to the south side of State Route 213 and quickly climb over the guardrail. Continue westward along the south side of State Route 213, again keeping the guardrail between you and traffic, until you reach the center of the large road cut along the north side of the road (Figure 16).
The road cut exposes the Century thrust fault, which places Binnewater Sandstone over Manlius Formation. The hanging wall contains a low-angle ramp which transitions into a hanging wall flat. Similar stair-step geometry of shallow ramps and flats in the Binnewater Sandstone can also be observed in a faulted sequence southwest of Tillson. The fault zone contains what is likely a horse of crushed Binnewater Sandstone and a sliver of Manlius Limestone. The footwall is a flat in the Manlius Limestone. The footwall is also cut by several minor thrust faults, the westernmost of which appears to be a wedge fault. Thus, the hanging wall of the Century Thrust contains the Butler's Lock Quarry. The footwall contains the Van Tassel's Quarry, which we will visit in Stop 6.

Van Tassels Quarry visible through chain link fence on the right

STOP 6. The Snyder Estate
This land was originally owned by the Snyder family, who were central players in the local cement industry since its beginning during the construction of the Delaware & Hudson Canal (Werner, personal communication, 2003). The Century House Historical Society now maintains the Snyder property. This non-profit educational organization is dedicated to preserving the unique history of the Rosendale natural cement region. Leave cars and walk towards the battery of cement kilns at the east end of the lot. Continue eastward along the small trail leading down a small slope and through a small stand of trees. Proceed along the base of another battery of cement kilns to the driveway of the small, adjacent house. This lot is private property. Please obtain permission from the owners before continuing along this route. Use the flight of small stone steps directly behind the house to climb up to the abandoned tramway atop the embankment. Walk eastward along the abandoned tramway for several meters until you reach a set of small cuts. These cuts expose shallowly east-dipping beds of the uppermost Binnewater Sandstone. Note the characteristic shale horizon (previously seen at Stop 5.2) and examine the well-developed cleavage duplex that suggests some degree of bedding-parallel slip.
Continue eastward on the abandoned tramway to Van Tassels Quarry, a section of extensively mined Rondout Formation in the footwall of the Century thrust fault (Figure 11A). Van Tassels Quarry is an excellent example of the classic Rosendale natural cement quarry. Mines are cut into the Rosendale and Whiteport members, which were historically referred to as the upper and lower cements, respectively. The Glasco Member, historically known as the middle ledge, is left un-quarried between the cement layers. If time permits, follow the tramway north along the front of the quarries. The Rosendale Member is several feet thicker at the Snyder Estate than is to the north and south. Continue on the tramway to the northwest, further up onto the embankment behind the small house. Return to the vehicles in the parking lot of the Snyder Estate from the north, along the top of the embankment. Pause along the way to examine the screening house (Figure 11D) and other remnants of the cement industry, but be careful to stay away from the large openings atop the cement kilns.
As we leave the Snyder Estate, note the Brooklyn Bridge ornaments atop the gateposts. Over 100,000 barrels of Rosendale Natural Cement were used in the construction of the Brooklyn Bridge because of its unparalleled strength. Other famous landmarks built with locally produced cement include the pedestal of the Statue of Liberty and the Wings of the United States Capitol Building (Werner, personal communication, 2003).

Note Shawangunk Conglomerate in road cut
Note Shawangunk Conglomerate in road cut immediately adjacent to the driveway of the Snyder Estate along the right (north) side of road.

Bridge over Roundout Creek

OPTIONAL STOP D: Lawrenceville anticline
Pull off on small turnout on left (south) side of road. It is possible to park vehicles here for a short amount of time. For longer stays, the public parking lot located just across Rondout Creek from this location should be used.
Leave the vehicles and cross to the north side of State Route 213. Walk to the center of the bridge over the Rondout Creek and look to the west. Although it may be difficult to see during the spring and summer months, this position affords a good view of the Lawrenceville anticline. The anticline is the westernmost major, map-scale fold exposed in the Rosendale region. The Lawrenceville anticline appears in numerous photographs taken of the Delaware & Hudson Canal in this region (Figure 17).

Outcropping of Shawangunk Conglomerate in escarpment across cornfield
Note the outcropping of Shawangunk Conglomerate in escarpment across cornfield on left (east) side of road. These rocks are in the hanging wall of the Snyder thrust fault.

Ruins of mill foundation along the creek
Ruins of mill foundation along the creek behind the bed and breakfast inn is supposedly the site of one of the very first cement mills in this region (Werner, personal communication, 2003).

D&H Canal Museum
D&H Canal Museum is located about 0.1 mile south of State Route 213 on east side of Mohonk Road

Blacksmith Shop where local dolostone was first burnt for cement
Blacksmith Shop where local dolostone was first burnt for cement located a few meters north of this intersection

STOP 8. Mesoscopic folding in Silurian strata, along the Rondout Creek at High Falls
Southwest of High Falls, the Rondout Creek flows roughly parallel to strike of the Rondout Formation and Manlius Limestone. At High Falls, the creek bends sharply to the east and begins cutting perpendicular to strike, down-section towards Rosendale. The highest falls are over an outcrop of the Rondout Formation. Downstream, smaller subsequent falls separated by shallow pools occur in the Binnewater Sandstone and High Falls Shale downstream followed by minor rapids caused by debris of the Shawangunk Conglomerate. As you follow the footpath past the High Falls power station northeast, note the shallowly northwest dipping beds of Binnewater Sandstone in the cut on the right. Once past the fenced-in area surrounding the power station, leave the trail and head north across the grassy area towards the wooded area long the creek. Stop to examine the millstones cut from Shawangunk Conglomerate placed as decoration in the grass. Also note the ruins of the stone building behind the cyclone fencing. This was once the processing-plant of the E.O. Norton Cement Company, which operated mines in High Falls and along Binnewater Road near Williams (Fifth) Lake (Werner, personal communication, 2003).
When you reach the waters edge examine the asymmetric anticline in the Binnewater Sandstone and High Falls shale exposed along the north bank of the creek. This fold is the westernmost mesoscopic structure in the fold-thrust belt near Rosendale. What is unusual, however, is that the axial surface of the fold is dipping to the west, a sense of vergence opposite to the regional trend. The shape and scale of this fold suggest that it is a fault-propagation fold above a blind thrust fault. The fault underlying this structure is most likely a west dipping back thrust associated with the merger of two detachment horizons in the Ordovician strata at depth.

Small road cut in gently west dipping strata of the Kalkberg/New Scotland Fms.

Old abandoned quarry in Onondaga Limestone
Old abandoned quarry in Onondaga Limestone in trees along left (west) side of road

Esopus Creek visible through trees on left
Esopus Creek visible through trees on left (west) side of road. Onondaga Limestone underlies much of this portion of the valley

Intersection with road to Town of Hurley.
It was here that the government of New York was temporarily relocated when the British sacked Kingston in 1777

STOP 9. Cleavage duplexes in Bakoven Shale
Road cut along State Route 28, west of Kingston: Our excursion has taken us full circle, returning to the foreland of the fold-thrust belt. Here we can see evidence of deformation associated with the upper detachment of the fold-thrust belt as deformation dies out westwards. The steep escarpment and road cut along City View Terrace, beneath the Skytop Motel, contains an exposure of the two lower members of the Union Springs Formation, which is the basal unit of the Hamilton Group. Here, the upper 10 m of the fissile black shale of the Bakoven Member grade upwards into the lower 23 m of the Stony Hollow Member, a sequence of the buff-weathering shale and siltstone (Ver Straeten and Brett, 1995). The structural relationships of this location have been described by Bosworth (1984) and Nickelson (1986). Numerous examples of mesoscopic-scale deformation are visible in the Bakoven Member along the road cut. These cleavage duplexes and shear zones (Figure 14), often less than 20 cm thick, suggest that blind thrusts cut the underlying strata.