Field Notebook: Maryland, New Jersey, Tennessee, Virginia, West Virginia, Indiana, Ohio, New York, Ontario 1907

Trip of 1907 New Jersey, Maryland, Virginia and Tennessee. doc.0093

Starter out with 400. I am here at July 27 " " 20 July 13-1907 10/ + 15 Massanutten July 11, 12 Bath Mountain " 14 Cherry Run " 15 Hancock " 16 Great Cacapon " 17 D. B. B " 20 Keizer " 24

doc.0093 Note Book of Charles Schuchert Yale University New Haven, Connecticut. 1907. If found by any one please return to above address. Trip in Descrip y Atlantic boder and Potomac - Murray section, and Tenn. with Reds.

date reid. place shipped from call. dates 2932 July 4 from Vincentown, July 1 - Jul 3 NJ 2933 July 6 from Harve de Grace, Jul 4 - Jul 5 Md' 2938 Aug 7 from Cambonleul, Md July 7 - 25 2939 Aug 3 from Louisville, Ky Jul 26 - Jul 31 2941 Aug. 22 from Cleveland, OH Aug. 12 - Aug. 13. 2942 Aug. 22 from Niagara Falls, NY + ontario Aug 15 - Aug 17 2944 Aug 26 from Sandusky, OH Aug 12 - 13 2947 Sep. 3 from Perryville, TN Aug 8-9 2948 Sep. 9 from Nashville, TN Aug 1 - Aug 3 2949 Sep. 11 from Camden, TN Aug 4 - 7

Phil Schuchert 1202 Linden Ave. Canton Ohio. Mrs S. Stutig 105J Academy Ave. A. E. Schuchert, 119 E. Leventh. Cin. Q. T. A. Bastriess. R. J. Luce. M. Corcoran, 57 Hall. New Haven, Conn. E. A. Callahan 472 Orange. " " J. E. Garage, Wtuna, Ill. R. J. Baslu. C. Q. Ohio. R. H. Gordon. Frank Hartley, L. F. Gille 192 Seneze St. Auburn N.Y. Mail to July 1-2 Vincentown N.J. Wd to July 8 Harpers Ferry, Va. Wd to July W Martinsburg " " Wd to July 22 Care J. P. H. Gordon. Wd to July 27 Nashville Tenn. Wd to Aug 3 Camden Tenn. Wd to Aug 7 Perryville, Tenn. After this care C. H. Gould, Norman Okl.

Yellows Correlation Table, Am. Rep. N.J., 1904. Remarks. Cork 1868. Clay 1892-1894 Yeller 1905 Siren sand, Fortis. 2'-1' Juffen shale Oak shale Seen shale Monasquan Mott D Manasquan Klaukonite mud sand 4'-1' Yellow sand Yellow sand Long Island C Vincenton Largely siren sand, Pliocene loam, etc. Clayey silt above at Red Bank. Bayberry beds above at Vincenton. Some muds have brims 4'-1' Middle shale Yellow sili silic sand Blue layers Clayey to mud Ceres Laurel Tinton Red Bank Marosid Patt Laurel Bermuda Red due to oxidized glauconite. 100'- Red sand Indurated grun Est Red Band Dark micaceous clay mott M in mott Red Bank Marosid Mott Franklin Columbus Brooklyn Muckville Lown sand, and sand. 30-50' From shale Quail Laminated lands Ma-Ta-man A Finds rather rare. 275 to 400 Not yet worked out. Raritan " Plastic Clay. Sand Upper Cretacous, 347'-400'

July first. Barrel, Reeds and Bottle at Philadelphia. First train on Long Island road to Vincentown. Stay three 3 days. Have the following Jokes. "Upper Cret. Form. of N.J., Delaware, & Ind" by Clark. "A Preliminary Rep. of the Cret. & Terti. Form. of N.J. by Clark. The fossiliferous "Jurra Marl" may I think be seen about Milton and also East of Grant Hollow. Ask after this at Vin- centown. If so take this drive from Vincentown.

Seem my Cecil Count has for roads and paths. [Look for unconformity, fact to occur between these formations]

Perryville, Md. Walk along P.R.R. track from Perryville to Charleston then across county to B.&O.R.R. and north to Perryville. Distance 14 miles. See paper "The Stratigraphy of the Potomac Group in Md." Clark - Kittredge. Section 1 1/8 miles E. of Principio Creek (P.R.R.) Recent Loam with gravel 5' Raritan Fine white sand. 11' Loam Brown loamy sand, bearing gravel at certain horizons base 12' Cretaceous Potomac. White clay, somewhat dim stained and variegated; at times graduating over into micaceous sands; changing to gravel, calcareous conglomerate horizon base — 10-20' Dense variegated clay. 10. Jurassic Patuxent under ground. Fogs Hill on B.&O.R.R. Potomac. Buff sands, water having off base 25' Dense variegated clay 10-30. In places with considerable pebble. The upper zone always with pebbles.

Lee opens the bed of Massawomen Mt.

Baltimore Ind. 26th School House, Hill, Lee J.482. Federal Hill, Lee J.484. Harpers Ferry. One day to see the immediate Region. Then to New Market across Massanutten Ont to Luray. Enquire here about driving across Mr. Leon Frontiers, Fork Cano Roads to Gordonsville. Then to Martinsburg. North Mountain. Stop at Martinsburg. Great Cacapon. Hotel here. A long section from the Medina to Ham- ilton. Enquire about cutting between here and Cum- bland.

de Clark's Physical Features of Md, and Schuchert Leron Devonian and Ontario formations of Maryland. July 9 wrote Sorden that we write from 12 to 74 days before we got to Cumberland.

Hancock. Also on the end on the other side. Cumberland. Look after Hartleys new localities. Then one day Cash Valley across to Devils Back Bone. Pinto section. One day. Twenty-first Bridge, Kezau quarries and Judge Allins. One day. Then to Nashville, Tenn.

Marville Tenn. Reservoir Hill and hill just N. & Here Orthorhynchula linneyi and large Leperditrias, a little to the N. are justly less than 20' Down are other quarries with an abundance of Tetradium and Cleunnaria. Naepli's Hill for an extensive section in Orthorhynchula and Tetradium horizon. The section is as follows: Upper Byogon beds or Rafinesquina zone. Then 20' down Orthorhynchula horizon. Then 12' down Tetradium zone. Then 15' down Soft chaly limestone. Then 8' to road. at South end. These are the Capitol Hill limestone beds of Jefford, the transition beds between the Trenton and the Cincinnati beds.

If anyone may also see the Oondog above the Diliurian or Lego yme = to Louisville, look here for Nucleocinns vermiculi, &c. The odonta demissa, T. perflans Phipidomella penelope, Nueleospira emeina. See Foerste "Dilurian and Devonian limestones of Western Tennessee."

Newsom localities. There is but one house at Newsom and I was never able to get permission to stay one night there. You may have the same experience so I would advise staying at Nashville and going back and forth to Newsom by railroad. The fare is small and the trains arranged conveniently for putting in long days collecting. The sketch below gives the best localities.

Camden, Tenn. Best Ovidian locality just on the out- skirts of the village. To the west of the village I secured nothing, or little. The chest is from 12-15 feet thick, overlain by shale 6-7 feet thick. Is this the Bloem shale? At the top is a 2 inch limonite band. Above this loose sand = Hardin? Ovidian sec. to Frontier. Forster gives the Camden here as 60' Heldrbug near Camden. South. One locality is near Chaseville on Wolf Creek up stream from the wagon road going from Chaseville to Holladays. About six exposures in a quarter mile from the road. Thickness about 20-25' Overlain by Camden chest, out croped only saw broken chest. Between 4-5 miles N.-E of Holladays towards Camden along side the road are two fine localities of Heldrubejian, 35' shown. Lowest beds have Michelinia and Favosites Bryozoa higher up. Phacops from upper portion. Forster gives this locality as 5 miles north of Big Sandy Station on the Lower Camden road.

Big Sandy. North of Camden. By wagon from Camden to Big Sandy and then 6 miles south to Tom Barnes is about 10' thick, a fine Hel dubyian exposure with Camden above. Above a recent lime mud deposit. See if one can drive direct to Tom Barnes and then to Big Sandy. The Camden is well exposed in a small station, quarry to the west of Big Sandy. About 2-1' thick. Spirifera and Eatonica common. It is often seen along the road the most western road for six miles south of Big Sandy. Forster says 5 miles S. of Big Sandy Station on the Owen Camden Road maybe also contact between the Hel dubyian and Camden. Pace, Henry County, Texan. Fourteen miles north of Big Sandy Station (1-1/2 miles up from mouth of Big Sandy River) to Saffords Williams Hill. The exposure is in Bexar County side, about 30' thick. Lowest layers Atrypa reticularis, Lepta Anastrophia followed by Orthocerids, with Orthostrophia (these are in the center of the Orthocerids). Phacops occur from and above the Anastrophic beds. Also Sophrentus. Pate called this locality Swoznes Old Hill.

One locality is under bridge at public road near Lashleys store. See for the boy Her Lashley, Pace, who sold me fruits. at 75c per box cigar. Another locality at old mill site about one mile above (? Smith). Pate said get team at Big Sandy Station. See Arthur Williams site Forrest says Camden maybe can see 20' thick and more. Perryville. Heldoutugian (Linden) On railroad Camden-Lexington-Perryville [the next page] [illegible] An abandoned r.r. track leads to the Linden quarry along the river. The clay locality in the northwestern edge of the town is harder to find but go to the last line of houses on this side S and look along the road for Li. Lazure

Also see railroad cut between Perry- villes and Parsons for Heldeburian. This 3 miles east of Parsons or 3 1/2 miles west of Perryville, Penn. Fine Camden chest nuts at around Decaturville which is one mile east of Perryville. Decaturville. or rather Decion Spring Parsons collection once made in a radius of 5 miles around decion Spring, located on the old Colonel Brallie's decion farm, 3 miles south of Perryville. This is the "place" here a "mans" home is the Brownsport (above the Balden) = to the Louisville. Brownsport Landing is about 5 miles S.E. of decion Spring, and 3 miles N. of Vice Landings. The Brownsport consists of whitest clays and 20ft limestones usually found in the open "mountain slades". Can easily be seen in the topography. Decion beds below are red, dark the slades. One of these grounds a 1/4 mile N. of home of Noah Butler, on road from Vice to Perryville 2 1/2 miles N. of Vice. Another 1/2 mile farther west.

93' throti lea. Others eastward on road from Dixon Spring to Tenn. River, many miles and S.-m. of the spring within a radius for mile. Those between Dixon Spring and Perryville are mainly in the Blendwitz and Dixon zones. The section here is as follows: Hardyia vestita . 3 = Bridgman C andr. 60' at C andr. Canadea chub [illegible] Pyrum Linden li. from a Rock with Cameronia Brunsport 100' after foot aft the li. onth shes telar. Oathaeospongia atre. Dixon clay 30-45' Red clays with Fistulifera Zepf li. 30-45' = Lriceville li. Baldum. Pyturn Landing at White Duffer Springs. Here is a fine third section of Helderbergian 100' thick. See Forrests p. 683. If time is at hand for here.

Perryville. In the quarry 1/2 mile N.E of the station is found the Branksport telar followed by the Linden = New Scotland. It is as follows: Linden base has Orthothetes wolworthanus, Pholidomella mata, Athriofora visa. Lower third of Linden 10 1/2 ft. Ashy crinoides rock with few fossils. Middle third 11 1/2 ft. Richly fossiliferous. Jasper rock, fairly crinoides with clay beds. At base Stropheodonta kelli, Strophonella punctu- lifera, Q. wolworthanus, Dalmanites mi- curus. Key new Uncinulus schucherti. Above this fossil zone there is marl clay with many small brachiopods. Upper third, 15 ft. Fossil clay. Exposed in the northwestern corner of the town and is overlain by the layers of li. full of byzogens, is a bed 1/2 ft thick. Sandy bed above which may be the Hardin sandstone. Camden fossils about Perryville are loose and from the iron ore quarries.

Tuesday June 25 - 1907 Brooke Botanical Garden. Museum building. A grey brick building with pillars of sandstone. Approach from each side around a central fountain to central doorway. In this like the museum at Prof. Effective. Three stories, 2 above ground and one very and one below. Basement for botany, First floor Economic Botany, second floor Systematic Botany. Windows high above floor double with transverse window a transoms. Piers about one-half the width of the window. Floor plan as follows:- Supporting pillars opposite piers, above case built under them, hollow inside. Floor both marble and tile. Inside color white. Cases oak,

"In the systematic collection but one four parts of each family is shown and these are the illustration in black n color. These are on a lead around rock-ground framed in oak as follows. sheep frame depths of case. Exhibits in first forms an orchid) Effect not pleasing. Outside case labels. Zoological Garden. They use a wall to one (directed) showy one of the polar eyes on the usual. Like about 10x12 feet. Good to show distribution Printed by Matthews - Mottling books, Buffalo N.Y. Alligators young and old this life day so into the crate to cool off. Coming in land the orals lie on their lips, the front two digits from the back one only plantipode. The walk boy and sadly, about ten steps a less than the cat

in their belly. In the orator which is very shallow they also use their lips for propulsion but it in here chiefly the tail. This is lashed from side to side just as a shark does. Join the use of the tail that has produced these huge and powerful swimming organs. On the land they prefer to crawl if possible, rather than to move lift on their legs. Princeton June 26-30-1907 Arrived here about 11 A.M. on the 26th and each day until noon of the 29th held entrance examinations at Lawrenceville for Yale. Had 34 men (18 finals and 16 prelims). The work is uninteresting but the men and the institution are the very best. Met at Lawrenceville Mr Lepry's father, the young president of Yale who called my attention to the base bones.

in the swamp near Saltm state. Another one is taking prelim exam here in jale, Philadelphia June 30-1907. Arrived here at a little after 3 P.M. staying at Hotel Shannon. Spent a few hours at the Judgical gardens, with a Reds in the evening walking around the city. July 1-1907. Spent 1/2 at the Philadelphia Acad- emry and Reds ad Ntite, At 11:00 ooth Dinner, Reds ad Ntite left of the Market Street Ferry over to Camden ad then for Vinclntum when we arrived at a little after 10 clock. After lunch walked out at once to the meal diggip.

2932 Vincentown July 1 - 1907 In the upper shale above south of Vincent- town the following section may be seen: ' Soil about 12" thick 3' Lying different imbedded bone. About 3 ft. irregular surface. Pleistocene Marine turns fossils. 3' Darker cylindrite, iron bedded. Petites scattered. Large pieces at bottom. One about 1/2 inch 1/4 wide and in length. Lignite. Hard piece. 4" - 6" Cretaceous Manasquan. Green sand with small Eoogyra, found seen, Shells teeth. Blancanite due for fertilizers. "Green shale of Upper Mail Red." or the same shale of the Manas- quan. Then walked along stream to beyond the Mill to diggings in the lower shale of the Vincentown or the upper member of the Ramerosses. These lime beds are just below the yellow sand and the basal horizon of the Manasquan. The Vincentown lime beds are not less than 15 feet thick, replete with Eocharia. Other fossils are rather rare are particularly the echinids, be picked up several and of the ones seen seemed at least two good ones John B. Brick

Vincentown July 2 - 1907 Started out early down the stream to look for other ex specimens. Saw no other fossiliferos places than the one of Saturday. Walked to Lamberton and then to Mt Shelly once or took the train at 1 o'clock for Vincentown. The county is or generally covered by the Pleistocene mantle that it is rare that the Cutler clays come out. In the vicinity of the Ranocross stream the country is a little hilly but otherwise flat and monotonous. A real agricultural country however. Later in the afternoon revisited the Vincent- town Byggra beds and finally found a perfect of circular echini. Found ten more a less good specimens. This locality is near the top of the bank about 150 feet up stream from the log over which the stream is crossed. This locally maybe found thus:-

doc. 93 This July 2 sketch map of Vincentown tops is wrong. He has Mill & Main St. & Hotel all o.k. with North toward top of page. But - everything else is wrong. - see [17533] + doc..... C. MacClintock 1992

Vincentown July 2-1907 [illegible] [illegible] other than and at / to Pleis clear stream flat count [illegible] town of soul the one may AGE: MAJOR AREA & MAP ORGANISMS: COLL. OR LOC. DESCR: [illegible] [illegible]

Vincentown July 3 - 1907 Packed material and shipped me small box via express. In reading Clark's notes on the New Jersey Cretaceous one is impressed with the abundance of green sand or fluenite. In fact all the formations may be said to be in the main of this sand. As one goes south the beds become more calcareous. Barrell thinks the Cretaceous shore line may have extended to the Blue Ridge in which case it must have also existed in the Great Valley but not to the west of the Alleghanies. In Connecticut it extended to Hartford. The argument for this greater extension is due to the way the Connecticut cuts across the Crystalline structure. It could not have done this had then not be after Cretaceous over, into which this river had cut its valley and as these were stripped away it began to cut through the ancient rocks below to keep its shortest course to the sea. Left Vincentown at 1.35 and Philadelphia at 4.46 arriving at Pottsville at 6.15. After seeing the hotel concluded to go over to Havre de Grace where we came at 7.30. A good country hotel.

2933 Horse de Gras July 4-1907. Set-up at six, a bright and delightful cool morning, this the birthday of one country. At the rail-road station (track A R) Principio is a sand pit with the following sections: surface yellow(ferrous?) loam, irregularly balled, 1-4ft. Maybe a laguna deposit. Blue-white silty clay, partly fractured, 1-4 inches. [illegible] stiff, coarse, clean white sand and a few more rounded, small pebbles. Argillay balled, Cross balled. Loose sandy loam with some marked head sand. 7 feet deep. The contrast between these beds is very striking. The lower sand in the basal Potomac (Patuxent) and looks most like a coarse head sand that has not been worked dry dry. Then a sudden change bringing in the layers of plastic clay, followed almost immediately by another change, flushy of the plastic clay into angular lumps. The latter in the yellow ferrous loam-- if these are marine deposits they are on the shore. The white sand is more probably a head sand.

"See section on pg. 57 2933 P.R.R. In the cut 1/8 miles last of Principio Station. The "dense variegated clay" from rail road cut of that least 20 feet are very red almost crimson. These, are clays somewhat gritty and distinctly or rather mottled but irregularly variegated. Did not see here the white clay in strata gone. Barrel has clay of this Patapsco gone from about 25 foot above rail road track. Style of come in advance from clay samples of the Baritan. This is the Baritan that we find the iron ore. Farther east lower strata, the Patuxent comes in. There are more sandy beds, sometimes variegated, during an abundance of iron. These iron layers have at times considerable flaky remain for sandy nature. One large piece with a concave surface had a regular dotted appearance. Have some fragment of it and also some of the ovoid. The iron ore pure Barrel the idea of several iron segregation. There are also had evidence that the layers own cracked mud deposits, if in drift iron had been Barrel for the evidence this evidence that is once certain to establish the nature of them deposits to be rather cultivated, marks in proximity of the sea. In other case the Patuxent when I clear sand maybe 5 or shallows den, filling up a depositing continental deposits.

In general one gets the impression that the sea came in for a short time, deposited the white, orange, blue, angular andrite rounded pebbles with crystals, later followed by oceanic variegated clays [illegible] deposits by him. In some places the white sands of the Patux- at is full of rolled pebbles. These are when removed from their layers distinguishable from the Pleistocene pebbles in being almost white quartz while the latter are stained a yellow. At Charleston one took the orange sand to the H.R. and came on the B.C.R.R., a little east of Frys Hill station. Here of the west of the station one sees the variegated clays in one place deep red, maroon and rose but pastward the same clays are bleached to white or lead white color while several hundred feet still more westerly the dame red clay reappears. After going over the cut it is very apparent that the bed of the Patuxet are laid down very un- evenly and the nature of the deposits for are very unevenly. In one place in the same horizon there will be a sandy plastic clay which when rather dried the fusion shows much finer mica.

In some places it will be a most clay and in still another sandy, in still other places there are considerable quartz pebbles not much rolled but rather as the cones rounded. In this sands it is a fluviatile deposit from coming off a county of metamorphic rocks. In general the sequence seems to be as follows: Towards the close or at the close of the jurassic the eastern shore of North America was probably a low lying land with elevations not exceeding 100 feet and without any deeply cut river courses as the present Delaware, Susquehanna etc. The land was depressed some and a very shallow sea made its appearance depositing a basal zone of well washed angular sands with well rounded pebbles. Above this shallow sea was filled up or that while in places one had sand was deposited in other areas, these lagoons or rather deltas was deposits fluviatile deposits of mud and various alut clays. This condition became general during the Patapsco when only con- tinental deposits occur. Now a second shallow sea invades in places more persistent than in other but nowhere are there any true marine deposits laid down. This is the Raritan a Plastic clay of the Cretaceous. A third and decided out-

majence sets in bringing in an abundance of marine life (the first time). This is the Potowom or Tama River sands and this eutrajene con- tinues into the Eocene when the sea outside. Today I saw nothing of the unemformities described by Clarke between the Patuxent and the Potascer and between the latter and the Raritan. As the Potomac deposits are largely of continental origin it seems to one that these unemformities may mean nothing. Then again they may and but only after it has been shown that considerable variations exist in the planes, that either mud erosion has taken place or that the surface shows considerable decomposition at the formation of soils. The metamorphosed schismic = metarhyolite seen so much along the D & B. R. R. is deeply rotted and chemically altered. In some of the cuts this decomposed material or mud simulates the Potascer that I took it for it only the chance by Banell that it was the altered metarhyolite. The Drayland Quarry has cropped it also as the Potascer in two cuts north east of Jackson station.

Arrived at the Hotel at 7.30 and Barrel left for Philadelphia on the 8.05, he will face his mother and ship it by return to mom. Harace de Grace July 5-1907 Friday Packed trf for Barrel and left on the 8.48 for Washington P. R. R. On the way saw almost no Potomac depots until near Baltmore, South of Baltimore for ten miles are seen many fine reframes and most of these are near the city. Baltimore are great for six miles or so could be another fine place to visit. Arrived at Washington at 11 A.M. Then visited the U. S. S. I.. Your Riga, Bros as apron. Then up the Washington Monument to Mount Vernon. In the evening called on Miss Morley.

Washington Saturday July 6-1907. Visited the U.S.N.M. War Series at Rathbun and Stegner, in the afternoon visited Great Falls. The upper broads valley of Great Falls is very plain above the Falls. The new page is sharp and angular. The river sand seen here is coarse, and unassorted, dirty and of very varied signs. This nature we like the Patuxent sand seen on Thursday. In the evening called at the Cosmos Club and met Lindgren. 2938 July 7-1907 Sunday. Left Washington at 9.10 A.M. and arrived at Harpers Ferry a little before eleven. Then climbed the [illegible] Virginia Heights and had a grand view of the Gap. The Potomac cuts directly across the strilly of the Blue Ridge at Harpers Ferry. Then the Eastern Branch comes in and the Potomac diverts more to east and cuts North out at a considerable angle.

/2938/ The Hearston sandstone makes the two mountain ranges while the valleys in between are of Alynfham rocks. These are a much metamorphosed district making the Catrothian schist and into this has been pressed a granite often very coarse grained. This is these ancient rocks that the material of the Hearston is composed, a coarse grained grit and won free conglomeratic sandstone. This series and the Harpur's shale are much altered. As the basal layers of the Shennandral limestone are said to have Lown Cambrian fossils, the same also in the Centricter sand-stone, the question arises how far do these deposits extend to the west. Are they eastern deposits upon the western land? Certain it is that the Para-Trias refuses in them. Or the higher Shennandra limestones come in from the west and refuse directly upon the lower beds respecting the sequence and character of the Stockbridge limestone? There are questions of importance in paleogeography.

July 8 - Monday. Intended to take the 7.30 A.M. train for Washington Junction but by a curious mistake saw the train go with Reds but Adkine and I were left. Later Reds showed me his material. Contact between the Cambrian and Tassie he did not see but a short distance south of the supposed contact he came on the Petroae conglomeratic marble. This conglomerate is made up of irregular sized, and more rounded limestone pebbles bound together by a ferric cement. The pebbles vary from the size of sand grains up to those twice as large as a human head. This ore cements zone is followed by one of a sandy nature in which limestone pebbles are also found but here they are not held so firmly and weather out. Further east occurs generally red but also variegated beds of a sandy nature in which the grains are but more rounded or well assorted. Further than is found (Reds found it in its place) slate with cuticle tubes reminding some of Archthyceus and less of Coleothus. The entire material is derived close at

hand, as the largest rocks in the conglomerate are nearest the Cambrian and become smaller forward. The dip in the sandstone and red shale from the car windows look as if 20 degrees backward. My wife and I walked along the B. & O. R. R. for about 2 1/2 miles to see the contact between the Cambrian (Antietam sandstone) and the Shenandoah limestone. While we did not see the contact, yet the fault line is once marked for on one side is the rugged relief of the Antietam sandstone with the higher ground back of it of the Shippens shale, while on the other side is seen the very red soil of the lower ground with its undulating surface. The latter is the ground of the valley and of the Shenandoah limestone. Examined all the surfaces along the line of onward but saw almost nothing of an organic nature. Nothing determinable. Not far from the Antietam sandstone was seen something suggesting crinoid stems and the quarry nearby for sections which may have been small Orthoceras. Still farther

and saw nothing to support anything. In some of the time culverts show on the white limestone two Lepidodipter and a small ostracod and bygma. These certainly are of the Upper Devon Rima. The limestone is said to be from Hayestown Md. This then is about the same position in the valley as Martinsburg, Latm. These limestones look ble- cidely like those of the quarries at Martinsburg. With the Rhemandral limestone thousands of feet thick ending abruptly at the fault line beside the Antietam sandstone the question is at once asked how far seaward did this limestone extend? Certainly across the South Mt. Blue Ridges on the Castoctin for limestone is known to run beneath the Jura Trias of Maryland. Has the shore to this area as far east as half way on the Piedmont Platform, the area of the surface uplands arcs nor seen in the metarphyllite. Suggestive of all this is the fact that the US Survey maps Rhemandal limestone to the East of the Catoctin Mt. and over which lies the Triassic. Furthermore farther east is seen the phyllites and crystalline limestone

which now seem to me like nothing more than the Mississippian Cambrian and Ordov- cian strata nearer the shore [therefore different] physically] and in the center of elevation, are greatly metamorphosed. The real shore line for these Cambrian and Ordovician strata lies in the region of the eastern Piedmont for here are seen surface flms of lara - the oreta- chert like. Left at 5:38 P.M. for Lunay. First over the B. & O. to Shenandoah Junction and then via the Norfolk and Western. Arrived an hour late at 9:15. Stopping at Hotel Lawrence. As one cross the Valley one are in the limestone and the land of abundance. Nothing can be seen of Massanutten Mt. for an hour and then the north end looms of sharply and in the evening lights a dark flue. As one go on it is seen that the Mt. is made of 1 several ridges. It is a remark- able case of persistence of rocks - an outline - in a limestone valley due to a deep say in the valley syn- cline and the final prevention of removal is due to the Massanutten sandstone.

July 7 Tuesday Luray Va. Shaded most of the morning Visited Luray cave pm 8 to 10 A M The cave probably have a depth of 150 feet and is be- neath the surface from 20 to 120 feet This in the Shenandoah limestone in the rhythm bedded zone (a conculent like beds) seen yesterday about 1/2 mile north of Antietam same stone north of Sharps Ferry, Queens, only me sees a fissure but once after the water has deeped down through the roof. The cave drips but little and may be regarded as a finished cave now on the healing down process In many places especially the dry places the stalagmite is exploding. The ground color of the cave deposits is a yellow but in places there are perfectly white deposits. The human bones seen some of which others de- termined by Zeedy, look to me as if they come here for effect, In some of the chambers the stalagmites are small and cylindrical or pointed, in others I just fluted pillars and finally there are roofs with an abundance of dead or hard like deposits.

After the rain in the afternoon walked south of Lanes. We saw but little limestone of the Keenandock, the lown hills with bands of that weathering into a deep red clay. At about 1 1/2 miles south or came into calcauries sandstones also with that bands evidently the Artictam sand- stone, Here then the transition seems to be com- bated from the Centietam to the Keenandock. I saw not a trace of a fossil. July 10 Wednesday. Fort Cross Roads. Eastern Brook Left Lanes at 7.30 and went east down over the Keenandock. The surface with many small hills, A little further down the slope to the river encoun- tered an extensive shale zone in the Keenandock. Arriving at the river it is plain that the stream has cut down its entrenched valley very recently for after rising towards Massanutton and looking well one sees that the topography on both sides of the stream is young. Soon are encounter the Chantinsby shale with the entire surface covered with rounded boulders of a quartzite = Massanutton. There were also

seen on the eastern slope at levels only 200 feet above the stream, coming up the mountain and not very far from the first evidence of the Massanuttes I collected in the Hartnessburg shale Triarthus bachi, Trimuculus concentricus and Pleumutilus. This indicates the typical section and I judge the design to be less than 200 feet from the Massanutten are possibly not more than 100 feet. Towards the crest of Massanuttes but we see the decidedly cross bedded white quartzite. It is a clearly crushed, white, coarse grained quartz- ite and gives having fossils that are not very numerous. The evidence as to source is clear and further - that the material has gotten from a great distance. In the Fort Valley south of Editz we saw a high exposure of Hamilton standing nearly vertical. On the bedding faces I saw in abundance Spiri- fer mucronatus, also Trifidellus carinatus, Chor- tes coronatus, Pleurotomaria (the common Louville form), Aviculapecten and Phacops rara. Second quarters at Fort Gas Roads with the lady running the store.

At 2 P.M. started out on an exploration trip, on the Leroy Fourtains road. Soon saw some Hamilton fossils but did not collect these for the present. At Leroy Fountains saw excellent exposures on two hillsides of the Lewistown limestone. This is the locality described by Spencer. The soil over these impure limestones is red as is usual for limestones in this county. In the soil cover are horizons of more fine limestone are seen siliceous fossils—about 3 species of brachiopods, 1 a Stromatypa and 2 sp. of cephalas. In other horizons lower down may be seen other fossils among them stromatoporae. Spencer gives the thickness for these limestones as 93 feet and all belong in the Oranlias — the same Marlies seen at Carl Valley are else- where about Cambaund. One horizon had consid- erable evidence of cytiden in columns and estalby plats. Above these limestones are soft shales that weather out some check. In the shales I saw Candelia and ostracoda. This may be Lower Oristang. Saw no evidence of the stelden hujon nor the true Oristang. (See later notes) (This one is the Onneldgs shale of Kindle).

July 11 Thursday. Fort Cims Roads, Virginia One quarter mile east of the Cornus is a fossiliferous exposure of Hamilton having Chorictes cornutus, C. ocellula but with sharper striæ, C. angustatus common, S. medialis one on each hinge and ethmoid lit. mucronatus), S. granulatus (rare), Tropidolepis casinatus (common). Michelinia lenticulare (for form common). Fontacalite (small, common). This locality continues for another 1/8 mile and takes one into the centre of the so-called Jennings formation as mapped by Spencer. All is unmistakably Hamilton. Then walked over to Seven Fountains and in the following three hours made these observations: All of Spencers Seven Fountains Lewistown bottom of 93 feet falls into my Menlinus as seen about Corn- Ireland. In the middle comes in a cherty Above this section a conglomerate of about 1 foot that now breaks out as cherty lites.. This is Spencers Country and is to be included in the (? Drift). Then across the strike for from 100's to 100's occurs a soft olive colored somewhat sandy shale, having various dips. Once once measured but got mixed from the dip line about 30-40 degrees. In this shale some

(at first thought the dip to peak are made out the thickness as frm 100 to 200 feet, but the dip is plainly not feet) distance above the true Hamilton Lepta- crinia Shellite, Phacops and crinoid columns (there left those pries). Then at crossing other horizons higher. sans Crinlia micolata. Smashed lower than the Leptocrini some hole found Dalmanella plano- convexa and Phacops. All of this indicates [Ordiary] but nowhere did a single Upper Ordian species turn up. While at work about North Mt and Cherry Rd changed the corelation to Kimpton. The trouble is that this eastern horizon is from some 1400 feet. follow away these beds came in thick black smooth shales with Stylodonta and Stephanja markers of the Marcellus. These beds may be 100 to 200 feet thick before the higher Hamilton or true Romney occurs. Broken for ponds but saw only Cystina hamiltonensis. In any court looking along the strike the locality takes one to the place on the road side having the Hamiliton finds collected this morning. The contact between the [Ordinary] shales and the Marcellus may indicate an erosional one for Middle orleded along the conglomerate layer and in 1500 feet noted that it came another one foot for heavy bedded limestone that at the other end was separated from the limestone by shale by 20 feet. If this observation is correct the Marcellus surface is concave as the true Silurian may be welded away. Further picked up a bris

I gathered limestone to me face I shield some attached fossils like those of the Osceola conglomerate layer. What in it is a Spirifer mud like S. [cyclotera] and valves of [Merrittella] or Renssi- [lauria] filling the former. Can this have been carried on the Beer's limestone down from wherein in Bath Mountain? Later - this certainly was a piece of Secrest li. indicating that there was eroded off out hole. The fossils attached to it show like those at Cherry Run. Setting over Massanutten Mt. and going down Upper tr Overall is less than 30 feet beneath the [Massanette] sandstone we found a taut of Calymene, Athys tes- [tudinaria] Byssocrinus micoleta, Rafinesquina alter- [mata], Tentaculites (about 3/4 in lay straight), This sandy shale zone must be at least 30 feet thick when one sandstone of considerable thickness affords (Faulted down upon Massanette sandstone) a character like the true Massanutten. A more shale of the same sandy character and Clathus testudinarius and Rafinesquina alternata. This is the Upper Massanutten faulted down. The sandy shales beneath must be his Lower Massanutten, the fossils of which indicate it to be Lorraine. Later in going back up the mountain collected again in the soft yellowish sandy shales underneath the [Lower] Faulted upon Lower Massanutten sandstone are found S. Athys [annulata] dorsal valve, several Rhynchonella

Lingyi (some very large ones reminding of Platystrophia but here too many plications or ridges and sinuses, &c), Orthis testudinaria, Q. one very flat, reminding of [illegible] emacriata and Rafinesquina allometa. These beds are from 70 to 95 feet beneath the down faulted Lower Massanutten sandstone. The latter comes in as shaly, a white sandstone decidedly conglomeratic at base with pebbles of 1/4t. 3/8 inch, Just above this lower (downfaulted) Massanutten sandstone I have collected Triloculus concentricus, Calymene calvicethula, Plectambonites sericeus (very common) Orthis testudinaria (looks like ovella and the striae running out on the large line). This horizon therefore occupies WETTERON lower in the faulted part while the solid one beneath the downfaulted lower Massanutten is certainly Lorraire, In the Lower Crystal Gap Taonurus are snailings. These on the road side just east of the stream. In the Monalies at Iron Fountains I once found large Favosites heldbyriae (smaller enallite) up to 8-10 inches in diameter,

July 12 Friday Fort Cts Road to Dorchester. Just a few steps out of the corner store at Fort Cts Rd we see up close with a little difficulty reminding of the Etheca form of D. mucronatus. Also sees what looks to be the true form and me Trophidostepus coronatus. Also Charites mucronatus, C. near coronata and Hysterodonta of the hemispherica section but not you are wide square. These beds must also be Hamilton. Nothing decidedly Hanbury. Just an 1/2 mile further out we see the regular Hamilton again with D. mucronatus, Cyrtaria hamilton- nensis, Charites scitula, Phacops bipr, Plurimfectum demissa, Mucarda, Paracyclas elliptica, Spirife granulifer, a rush of a large coral like Acervu- laria davidsoni but more probably Cyath. Hyllum caespitosum. Here we again see the smell from D. Spirifera mucronatus. A few yards further out we see a large thorny Leptostelphis seplana, Hysterodonta demissa, Crith- elinia stylifera, Spirifa mucronatus, D. granulifer, Crinoids (have some pieces), Streptelasma rectum,

"The road then flattens out and we see nothing to de- termine until we came to the many portion of the Massanutten. The Out, and then crosses the creek and we see the strata [Little Fort Valley] dip the other way, i.e. east. & the very marious really are we on the varigated hills (red an green) of the Rockwood. [29832] Then across the last portion of this mounn valley when we again come upon the Rockwood. The rise then is long and gentle to the top of the ridge when the Massanutten outcrops and we have a view of the broad ad beautiful gravel ruddy of the Shenandoah. The red Rockwood just above the Massanutten gives one the impression of continental deposits in their marrone red color, peculiar mithering, absence of joints and the unmistakable presence of sem-cracked surfaces. We saw large outcrock faces with these crecks are a great probably not less than 10 feet thick. The lowest hills are sandstone followed by red shales. In the Massanutten near the top one sees occasionally layers of inches thick and rather large boring-James' dolithus. But we saw no Arthur plgeous. In looking back over Fort Valley one sees the good skyline with the Massanutten ridges to the south ad north. Between lie are the strata from the Rockwood up to probably the base of the other co

"This valley is canoe shaped, i.e closed at and widest at the center. The same is also true for the Little Fort Valley but on one hand I this morning saw nothing I struck higher than the Redwood. At the crest of Mount Massanutten Mt. overlooking the Shenandoah Valley here as in the eastern valley one is impressed with the log of hors members of the Shenandoah and the moist nature of this river in a fairly flat valley. The river is now seen to be cutting considerably fast in many places we see the rocks crossing the river making riffles. Across the river valley the land gradually rises to North Mt, which also not a little south of Laurel Creek, but if it is a higher Little Lively Mt. rage also decaying out just below horndstrock while still North Mt. further east is a higher range and large than any of the others. Coming down the mountain one soon sees the upper candy members of the Mountain Lily and Dalmorilla testudinarie. About half way down the foot side within 100 feet of the spring and trunk for horses (I)ike collected Dalmoralla testudinaria, Refnerguina alternate, Taronculus concentricus and especially common Plethuromitis senicus. This is the level of 1350 feet above the sea. The same holds with mi-

nucleus continues down to Mt. further, At [altitude] 1950 feet, I picked up heads of Toxithurus brevi. [altitude] At 950 feet Reeds and I picked up several specimens of Diplocidatus and one Leptobolus having her four radiations. Ten specimens. This locality is just up the mountain from the turn in the road at which one has a fine view of the river bridge over the Sheanum- drah. There is more Haell shale at the bridge, (Later, The same formation found at Martin's Ferry at the base of the Martinsburg shales) There is no finer nor more continuous section of the Martinsburg shale than this one in the road from Dorodstock of Massanutten Mt. thin (one foot) one exposure beside the road from the bridge up to the Massanutten sandstone. As far as I can see the Martinsbury trying to the Utica and help in the Lorraine with Orthorychule being as the highest design member. Throughout it is a black sandy shale that weathers into yellowish, red, white or mottled white and black shale. There is much fine sand and evidence of minute cross bedding. More sandy at top [illegible] from Massanutten. Crossing the bridge and walling to Dorodstock one passes down more Martinsburg, all black, to the finer size of the sand about 1/8 mile from the bridge, here the limestone comes in. In

the stone walls alongside the road saw in the dense non crystalline limestone the following: Dimorthes pectinella, Prasoporia the large form near 3 inches in diameter, Cyclorhizus a Pascerus (common) an abundance of Monticuliferos, and evidence of many gastropods. This design = dimictic (1975) is undoubted in the Middle Trenton. There- fore all of the Oratunian must occupy the horizon of the Utica and Frankford. The same Massanutten equals the Lorraine. The low lands, then solution, and the debr sition of great limestones came to an end towards the close of the Trenton. Elevation set in at first (can I anticipate or confirm my next elevation?) gently changing the chemical deposits to one of detrital deposits a poor sea of quick deposition in fine sandy deposits blackened with the destroyed organic life of these deposits, and the cause for or little deposition of the life of this sea. [illegible] The elevation continued and towards the close (= from Massanutten) of the Lorraine the sea had vanished from these parts. Elevation still continued during Richmond time a poor regolith during elevation had been made and was ready to go to sea when the land sank back some as the lilyman was wetted in. The rivers now began to carry out

"This in large part derived from Devonian geology" at maximum elevation. The coast and into this shallow sea was deposited the lead sand making the Manawatu Upper The cycle is now begun and the sea while not constantly advancing upon the Blue Ridges was at first filled up more quickly than subsidence took place and so the first deposits of the Redwood give evidence of just sea marsh flats in which our deposited red deposits, which at times were reared to the sun and cracked. Plenty witness- dence set in but at no time in the Diluvium was the Cumberland gulf a normal sea with an abundance of life. All through the Diluvium along the eastern shore the sea was muddy and not well adapted to an abundance of life. While this elevation was going on, begun in the Utica and dissolving the sea from this region towards the close of the Lorraine, the sea still existed further west. Here also due to elevation the sea was shallower than before and the detritus of the elevating land - a mud - was being carried out by the constantly elongating rivers during Richmond time making the deposits known as the Medina - the Red Medina only. While these deposits are not continental yet they are the sands of rivers in a shallow sea one are therefore not affected.

[illegible] [illegible] by me the in co [illegible] [illegible]

July 13-1907, Saturday. Brodstreet to Martinsburg, on the Southern R.R. Left Brodstreet at 8.16 A.M. and arrived at Martinsburg 11.15-- We go via Strasburg and change here to the Valley Branch of the B.&O. to J.T., Harper's Ferry, are then onk to Martinsburg. Martinsburg, In the afternoon followed east along B.&O.R.R. Not more than 4s miles from station came upon the contact between the Phocanclock- (?) and the Marti- s-bury. The limestone belws say 100ts 200 feet of live Leptolus, Orthas tricenaria and Strphomene crebescens. At the base of the Martinsburg immediate at contact collected Chimaerographa typicula, and thus or more additional species also Leptolus lepis, The beds dip 35-0 E. Have a photo of it with a crust on the face of the limestone. The limestone begin to introduce thin shale gives about 4 feet or thirty. There became more numerous and the all shale with considerable carbonate of lime in the shale. The transition is gradual, Twenty five feet above the contacts pressure has so jointed the shale that in forms can be seen. The limestone where the Martinsburg rests on it has

by marine conditions of life but only by the physi- cal condition of mud spreading in regular - four regular beds. By the time of the Marlins low lands once again the rule and the sea deposits in the main limestone. Coming elevations indicated by the muds of the Helderbergian and the climax in the OsirKang, as is to be seen later at Hun- crook.

Idealized section across Massanutten Mt. from East of Lemon Fountains to Brodstock. This side also has a small valley as on the west but less than 1/3 as wide. Eastern Sheanandoh Valley, Eastern Branch. Fault. Up Mount. Low Mount. Fort Valley. Fort Cren Roads. 2400 Hamilton ? 300 Kingston 90-150 manlius = Lemon Springs = ? 710-858 Rockwood = Oldtown 500-500 Upper Massanutten = Ordina 200 Lower Massanutten = Jordan 2500 after Abencer probably about 1000 Martinsburg Chanticleury just out the Otter River li. Little Fort Valley, Rockwood m Upper Massanutten Lower Massanutten Western Sheanandoh Valley. Eastern Branch Sheanandoh limestone. The limestone where the Martinsburg rests on it has July 13-1907. Saturday.

a dip of 30° to the east. Dr. roots 300 feet over the beds are nearly horizontal and still further west begin to dip in the other direction. This is then to copy of an arch. On the very large Ormsbury quarry on the upper most layers the common fossil is the little button like Receptaculites = Cyclotomus common in Tennessee, Frith are abundant but can not be counted out of the limestone. These recognized are Theftosoma arai- culum, Raphistoma lenticulare. In the light blue or grey limestone (breathing a milky white) saw on fossils. It is these conchi- dally fracturing light blue limestone in heavy beds that is quarried here on an extensive scale for lime burning. They end abruptly and then follows thinner irregular bedded and less pure limestones. Are all these upper beds (judging between 100 to 200 foot thick) to be regarded as Trenton and the light blue beds below the Homer River series? There is a very decided change in the limestone de- sposits at this horizon. The upper remains of our north while the lower brings to mind the Kirk Bridge region of Kentucky. In the lower li. same oph-diopseting. The [illegible] at the contact with the limestone shows it to be typical Utica.

"[Illegible]" Combined with the [Mananutt] results it runs up into the Zouaire. About 3 miles west of Martinsburg limestone appears again. Its lithological aspect indicates it to be the same series that undulates the Martinsburg near the city. If this is true the Martinsburg lies in a syncline and its thickness is probably that given by Keith 700-1000 feet. Martinsburg to North Mt. July 14th - 1907 Just west of Turn the heavy bedded white O. appears dipping a little south of east, about 30° seem to have begun and Geocimus. A 1/2 mile further once heavy bedded but in regular beds of dolomite with the same dip at 20°. At the first block turn out of Martinsburg about 1 1/2-2 miles out the dip is about 20° to the south. Less than 1/8 mile it is 72° E. There overbed bed continues for 1/2 mile where other we see nearly vertical beds (90°) of carbonate little limestone. In these dips cracks are common and are well seen cracked surface with the erosions. Filled with carbonite depose or even an impure celestite. On a duplication of the conditions we is the waterline at Piedmont.

"September 15-1908 Bird and Darin have this examined going down the other demand road valley. St. by the Lowville. Above eliza Spit (1924 fine in other run also - Chazy) In another place the ripples are very distinct about 1 1/2 inches apart from crest to crest and about 3/1 inch deep. These are the ripples of very shallow water. A few inches above this surface are unmistakable evidence of sun cracking, i.e., the coarse dirty plots are cracks from 1/8 to 3/4 inch wide. Most of them about 1/4 inch. This is a fine case I just shallows of marine origin, if a long mud! The calcareous mudds are one pure limestone (all this layers) are irregular in deposition but sparse far more regular than in continental deposits. These deposits showing all these evidence can at least 100 feet thick. The place is the first overhead major bridge and I Martinghway or 200 yards east of Taffs station on B.C.R.R. I again make those deposits east of Taffs and once more 1 mile west of the quick flush eight times. In all these places ripples marks and sun cracking is conspicuous. In places then is much disturbance and one faulting but the three or are seem to be my cliff. In nearly all the cuts through the limestone from five miles east of Scott Mountain and the strata are more or less vertical and those or seen all appear to be of these shallow water

deposits. The country rises considerably towards the mountain and the B & Q goes through the lowest part of it. In the cut through Pratt Mountain we started one word in the Becraft limestone where collected considerable loose fossils. We lot with the greatest abundance of Rhizidomella assimilis is from about ten feet of the top of the limestone, while the smaller lot is from a game about five down. The Becraft limestone is continued upwards by a shale series in which few fossils can now be had due to These shales there are clearing towards the top. the mountain matting. Chacops and a small cep carol are the only ones readily seen, but on breaking some of the limy pieces from # new the top of the series collected Styliolin ostracods, an Orthis and Ondelia. Have taken these fossils. The limestone has at least one gne (conglut.) The Marcellus Haell shale rests directly and sharply [distinct heart] on these Helderbergian strata. The two seem to be conformable but there where absent are of the Onitau and Ondopa. (the calcareous gne) Above comes in the Hamilton, near the base of which Reeds collected a slab with Spirifer zigzag, Orthothets, and Chanites (see

(in the concret may beds) sloth). Dr. [illegible] of Yale collected Torpidocleptus carinatus, a large Panetlla, and saw Spirina macromata. Yale soon determined the overturned nature of the syncline but at first drew it as an anticline. Ruds saw nothing more than an descending series [illegible] did not make use of the overturned cycine. Resting on the Beecraft Limestone is another badly crumpled shale series which at first I thought may be Salina. After some work collected on the dump to the north of the tracks near a farm house several specimens of Climacocleptus. The horizon is therefore Manuttsburg and the great overthrust fault here lies between the Man- tuttsburg and the Beeroffs. At this point there is therefore cut out some of the Holden- buryan, all of the Salina, Rockwood and Mananuttes. During south from Matt Mountain sta- tion to Hedgeville I saw in a stone ware of the boarding house on the hill Rocks of what appeared to be the Mananuttes and certainly Rocks of the red continental

little deposit of the basal Rockford. The ridge of Hatt Mountain is considerable high here and rises to the south and gives the appearance of having on its crest the Mas- sanutten quartzite. In other words the great over thrust fault of the valley refers on any Silurian horizon up to the Beacro. The following is the section (diagrammatic): Fault Slogmended Limestone East Onartinsbury shale. Beecroft limestone, Hurst fault. ? Ripton slate. Chard Slate. Jaw about 20=30 feet, Britany base Charnygan - Some Quartz beds. Measured 41 feet (see profile about this) Black Motal Granodite Marcellus, Lime stone of Trane Grae elcurans Hamilton. Forns. Erin free des Hamilton - 94 futs. Concretions Hammillth - 41 feet. Continued class Syncline at Hart Mountain, one mile south and Hatt Mountain at farm and O.R.P.

Martinstung, Monday July 15-1907 Cherry Run to North Mountain. At Long Run one mile west of Cherry Run may be seen the complete Heldebyrian section. Just on the east side of Long Run about 20 feet over of where the hill begins to rise above the track level may be seen the Marcellus with an abundance of Stylingia (at the top) resting on the Kingston. Thus as at North Butt, the upper beds are a little more calcareous and hold fossils of which we have a tail of Dalmanites, Phacops, Apectia [illegible] and a few other things (see fossils). Little or no evidence of the thickness of the whole cap is seen. On the Long Run there is a thin conglomerate and smalling, the base of the Kingston shale. Page 18th thick (laren pieces) resting directly on the Beech Creek limestone. As one gets up the slope of Long Run one comes in the neighborhood at once [illegible] and as the upper beds have an abundance of fossils among which are Rhipidomella (large ones requiring D. maculifera), Cassimilis, Orthotheca mordeniana, Spirifer ectopterus (in this right it is the Beech Creek forms) and other min de-termined species. This zone is about 30 feet thick. These limestone are heavily bedded with almost no shell parting and in places with chert (towards top). These rest directly on other somewhat thinner bedded limestone with much chert. These are the Maclellan beds in the New Scotland. These and

the Beccuff are one continuous series and there is no except from the slates. considered difference in lithic appearance between them. The thickness by stepping is 84 yards with a dip to the north of 30° This makes the thickness 100 feet. [675] The Over-Scotland fossils collected are from the base as has determined. S. macroplema, D. pulamellus, Strigtilasma rectum etc. The section is continued deeper with other thin bedded limestone but the series not well exposed. These strata are all on the down side of the anticline i.e. to the south. To the east the strata are in long rolls and about 1/2 mile east of Cherry Run the Marcellus appears at the surface for a considerable distance. Up to Back Run then the Hamilton appears. In a cut on the side of the K North Mountain the Hamilton series in a larncel as films. West East Concretions of 10 or 20. 3 feet seen Thin and regular halber zone Tripidofelus calipatus and fern fronds. Ophicula tenuis Max calcareous beds with many fossils. 41 feet. 20 feet seen. The limestone has in abundance Chmites optalis C. coronata C. scitola, Spirifer micrometa, Textaculites, Alor Spirifer granulifera.

"The North Mountain cut ends in the concretional layers of the Hamilton. This zone has considerable thick- ness and is seen in several cuts up to Howell Run. It is in this zone that the two limits of the syncline re-appear red out, Below it in the cut comes the then first markedly concretional seen in the cut beyond North Cut, an estimated at 35 feet thickener. Then the once coleorous highly fossil- grows layers having a measured thickness here of 94' Then the Marcellus shale having a measured thickness of. 158 feet (Undates thick concretional Marcellus) The outturns and clear syncline has its center in the concretional layers of the Hamilton. There is therefor no joinship or chemistry in this region. All the way from the Matt Mountain cut at its western end to Cherry Run a distance by road of 4 1/2 miles one sees nothing but the Marcellus - Hamilton in a series of low folds almost horizontal. As one approaches North Cut from the west these folds become once prominent until a quarter mile of the cut when they try to fold at high angles. In the fields above the Cherry & North Mt cut one sees their lies over the ground giving evidence of the presence of the Bereaht. The Bereah't and Chippewa here as at Cherry Run is separated by a conglomerate bearing stratum

dec. 93 July 15 Idealized Section on B & O. R.R. level between North Mountain and Gough Creek. (After L.F. Hile). E W. Shenandoah Martinsburg Limestone Shale B.&O.R.R Level Fault plane Upper Hamilton Marcellus Kintston, Backraft & New Salina, Clinton etc. Upper Mesianutun a Twcarria. North Mt'n. Cut Gough Creek. Exposure 1 mi W. of Cherry Run. Exposure

{ "text": "in the\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n\n [TRANSCRIPTION_TRUNCATED_DUE_TO_LOOP]

into a sandstone, the thickness could not be determined but it can not be less than 24 feet thick, therefore three times as thick as at Broyl Run. It is un- doubtedly this layer that appears on the Marlins Limestone at Leran Fountains in Drasenvuthin Mountain. (1921. That is the conglomerate at the base of the Orandagon lies on the Lower Regar.

Martinsburg, Tuesday July 16 - 1907 Hancock, St Va. and Md. At 11.18 left for Hancock. Going along the B & O. P.R. over the first strike encountered one Hamilton and then Marcellus. The dip is 1m (probably 350) to the east. Then follows the upper Oriskany or rathering down to a loose sand. The lower part of this exposure is a silicious shale with chert bands, actuating a yellowish-red, followed by a thick series of thin lidded limestones with shale partings. On the faces of the bedding planes saw many fossils among them, those that I can decipher from the lower part of the Coggmans or Meristella griseauntia. Orthotheca and one bel form, Tentaculite cyphacarthus, Bryozoa etc. These beds are followed by other of a nodular nature also with shale partings. None of these beds are in the upper Coggmans as one of the corals or Stromatopora are here but the fossils seem to indicate that the lifter beds beneath the Oriskany begin in the middle Coggmans. About half way down these beds found a good crinoid. The total thickness of these limestones shown beside the railroad track does not exceed 75 ft. (See account of July 17) The base of the Marcellus here more than

farther east is mac fossiliferous, Stylisina is abundant. Other forms are Ostrocodes and some Brachidiurids (see the lith). The Oriskany sandstone beneath the Marcellus was measured and gave a thickness of 64 feet in this cut but many fossils are seen but in the quarry they are very common. Among these Specifics are- Pera, Rensselaeria ovodes and Platyceras are most in evidence. How one can make this thickness 20 or in clints. The silicious shale (with chert) beneath the Oriskany was measured and gave a thickness of 67 feet. From the great abundance of large fossils in the white sandstone I should think this shale did not to hold the same position as the black Lower Oriskany about Cumberland. The only fossil seen was Specifics litotaphis. There is then here as elsewhere the absence of the Onondaga beneath the Marcellus. Beneath the Oriskany there is in this region a decided difference in that the Oriskany shale reposes not on the Heldeburyian but lies not higher than the middle Creymana. Therefore there was here a land interval eroding away the Heldebur- yian but I think this erosion was slight but that here, the Heldeburyian was eroded out by the action of the invading sea.

By rail-road it is about 10-11 miles from Stonewall to Cherry Run and while here there is no Cretany yet the entire Heldenbergian is at the latter place present all of which must have been present at Stonewall for the sea came from the north and yet all of it is absent at Stonewall. Of course in different places there is probably once in less of it preserved. In the first quarry operated by the Pennsylv- niania Glass sand Co which is high up on the mountain side, at least 100 feet I'm probably 75 feet wide and 100 feet deep one is im- pressed by the purity of the sand in spite of its many faults, and the wicker-like nature of it. This only the loose soft material that is used as the hardened layers have too much iron. About one third of the material is thrown away, the remainder is crushed, screened and altered to be used for glass sand. This also pulverized and used in roof making and by potters for glaze. About 120 tons of material is quarried per day and the sand for glass making is sold at about # 1.50 per ton. The Cretany sandstone at this locality is an unmitatable clearly worked hard sand.

Mr. Oistang doc. 93 At Hancock plan sand more the Oistang is 180-200 foot thick. Just a little east along railroad it appears like outcrop by fault. Told me by Mr. Stue. According to Rove a little further east it is 50-60 foot thick. April, 1908. in excavation with Stue

By rail-rail it is about 10-11 miles from Hancock to Cherry Run and while here there is O - x at the battery place. about $ / 25 per ton. The Christian sandstone at this locality is an unmistakable clearly marked hard sand.

"Originally it must have been more identical with lime because of the many fossils. Anything of the lime shells in life, all are casts. Then somehow in the great anticlines is a water gone and it is this circulating water that has taken out all the lime. The sand that is now present in places was probably brought in by the circulating waters. In the morning again visiting the great limestone quarry of Martinsburg, they have a depth of two miles. The material is largely used for road metal and flux for steel smelting. Some is burnt for lime, coal is used. In all the quarries the material is the light blue (or rather white) limestone. I even found in heavy beds beneath the then bedded uneven grained limestone. It has fossils but none could be made out. I was greatly surprised to find in or near a limestone a large serpent decidedly seen coiled. These are the higher layers, these or much less crude as seen in Lundy are lower in the section. These light-blue limestones often exposed in the

soil disolve readily. In one place I saw them taking out the red earth to a depth of ten feet. When or cleaned the surface has a decidedly Balk Lanes effect. It is common to see the joints in this limestone greatly enlarged by dissolution and going down for 75 feet. In some cases even Cavernous. These conditions are not true for the upper thin bedded series. About 1/4 mile east we come upon red sandy shales of a continental type (very much like Greeley) then upon a shale series and then upon a high called series if this limestone interstratified with shales, these are Michigan Algonquin miller beds. Tort a photo of these last beds but it is raining. out of place. Insert next page here.

Great Cacapon - Hancock. July 17 Wednesday. Took the 6:30 train to Great Cacapon and crossed the river to the Western Maryland R.R. at Tonolow- gay [illegible]. Here above is seen the Crisfay sandstone dipping about 30° to the W., with a thickness of about 200 feet (the dip being 200 feet at 45°). These sandstones rest on a series of weathering red mud shale in which occur Physopleura, Lep- teaene chondralis, Strepho edata beds. This Newark land zone is at least 30 feet thick but this is a guess as the place is much covered by trees. Then follows blue limestone, then bedded sand and shaly slate containing an abundance of fossils. There are the Creemans beds as seen at the R.B.B. at Cumberland. The section here continues into the Marlins which is more modelled in li. The thickness seems to be as of Cumberland. Above the Physopleura beds appear to lie beds of thermal shale. The strike are dip East. The lower delina beds are first red, green and then a variegated series follows: blue, gray, red and light yellow that weather yellow. Around the top lying shales appear. Below the lying beds are above the Rhynchomella.

for the clay shale series is much mud over worked so that are appear to be deposits of mud let over while the sea spread for time in time. This zone has the Cement series. A little east of Chiles & opposite Sir Johns about Rum on the B.C.R. some thin bedded quartz its in places a conglomerate appear and beneath them shales that have Clinton formits. The regular Clinton strata is here much larger than usual. Also saw the regular (narrow flims and branching) Orthothecis, and Rhizidomella (see if circularis) in the sandstone a Leptocodium resembling a small L. planocomum. Farther east at the Cement Mill at the top of Round Top can be seen the Lower Salina split almost every layer very cracked except the marble as it was used for cement. Here also is nicely exposed above the Canal road and again beards the Western Maryland track or fine folded and an anticline a just lost if it a syncline fold. Thus:- Red bed Red bed Cement layers.

"One is impressed with the beds above the cement horizon as being decidedly sun cracked. Every layer in a thickness of about 20 feet, along the rails on it, there are at times shown no foot sheets of just square are sun cracked. The bedding is far distinct to be of a continental nature and for the sun cracking indicates great sand flats referred to the sun. Flooded rivers and wind blown sea flooding must account for these accumulations. While we saw no marine life yet at Cumberland we find here an abundance of Ostracoda. The Red beds with their peculiar vertical green markings are the basal series before the cement beds and the mud beds with some crocs on land down. Later the sea deepens and the great coleorans series of Pints and the Sherdubays are laid down. Red beds for 12 feet.

July 18th Thursday. Trifles easy and write letters. Left Martinsburg at 3.17 and arriving at Cumberland at 9. Stopping at Sandons. Noble and Reeds at Mrs. Roberts, July 19th Friday. Cumberland, Md. Collected all morning up to 1.30 at East Valley. The section begins in the lower Martins shales and some limestone [illegible] about 75 feet thick. The fossils collected are amalgam for the upper ten feet, a few are marked as from lower layers, there are from about the middle.) Then follows a series of heavy bedded limestone with some Charnia for 30 feet. One limestone of the same nature contains for 25 feet abundantly in Favosites & Phyphyllum and Stromatolites. All of these beds are Martinsburg. Apparently nothing 30 feet thick Above is coral gone but Reeds and Noble found it of the field and rejected an area across limestone with sandstone. Can not determine the origin. In talking to Gordon of this horizon he thinks it should go with the Ordovician, above has some [illegible], Then follows the Lower Ordovician.

Billy Mt Hanmon Cumberland Sep 6 - 1908 The red Medina sandstone shows much cross bedding but in our sections. Cuts show one foot deep. Sand equal in grains then shales. In some layers irregular sided vertical holes that have more mud than sandstone, these are of organic origin but what do they represent. TJ F McNeut. White Medina Red Medina Bells Creek The Red Medina is a series of alternating sandstones and red clay shales. Red Medina without much rock into White Medina. The latter same into Clifta The White Medina is first a heavy bedded also fine grained quartzite with some cross bedding. It becomes thinner bedded with large beds and the mud shale are fine into the Clifta shales. Red Shales 6" sandstone depth colour 14" Red shales 4"

"Lone" section at Keyser. Thin redded chalk flues overlying stones. Reds nearly 2 inches, thins when overburdened. About 18 feet. A similar zone of shale lies as half a foot thick, central chalk flue lies in beds from 2 to 8 inch thick. 10 = 20 feet. Chalk flues overlying stones which are from 6" to 24" about 18 feet. Shale zone 4-5 feet. Dark flue lies overlying a bed of shale from 2" to 24" 120 to 135 feet. Seamers line prime tells almost into a magnesian Leda horizon of Judge Bell via R. Camellion zone. End of quarry. Bottom. The lower layers overlie into the red shale, li. & flow in a fauna similar to the Cape Longington Valley Marlton, Rhynchonella mephitic. Byzans, Rhynchospira and Ostreoids. See the little faunal collection above. Shales here shining foraged. Now the difference in the seams to see the Red Granite and the White Tuscarora. The Clinton shale forms the base begin to introduce their white sandstone, then there reds and shales and formed all in a clean white fine grained well washed sand, now as quartzite, some grass bedded rock and much. The Red Beds of the granite at the base (as exposed) have more shales than fine grained sandstone. The sandstone often as much as one of the shale beds, have handsome reddish streaks with hornsp. About 50 feet beneath the Tuscarora the same stone layers take on the shell features of the white white sandstone, and there are some of the transverse streaks. Towards the greater if the granite with the Tuscarora the sequence in columns. Heavy bedded Tuscarora not quite white. Granite bedded red slate sandstone - 3' Shales - 4' Red shale - 1 2' Sandstone - 2' Shales - 2' Sandstone (slate colored) - 15' Red shales - 20' Thin bedded sandstone with flake structures - 32' Red shales - 6' Sandstone lighter colored - 14' Red shale. 4' In the course of the shales remain the same red but the sandstones are grained to almost white.

There is no deposition here between the Junicta and Tuscarora, It's a complete sequence fancy without break upward into the Clinton. If one is Silurian then or are both. As one goes up the hill higher into the Tusca -rra the sandstones become whitish, craggy and more fine grained. In other words the sequence is complete from a dirty muddy sea to a clean head sand depositry sea. July 20th Saturday Cumberland, Md. Rained all night or started out late at 9. Spent the day out. Start by at the D.B.B. Made a general collection from the beds in the Cregmans and Shanlens. The bed of my published section labelled 3c is disturbed, a few cracked ones. These are my comprehensions of the Bock Dome June 22 foot thick. The New Deal land geine appears to be about as thick here as on the opposite side of the Creek, but more than 10 feet of the chief layers with thin accerflums are seen. The surface is thus crowned for about 35 feet over the Hackleburg.

Shales of the Lower Ovislay appear. In these beds I saw Leptocidii Helellites, L. finihista, Orthothelis (on specimen) and the new species described by me. The second one is probably also A. Grill. The erosion of the Heldburyian beneath the Lower Ovislay is decidedly different between here and Cast Valley. At D.B.B. only 10 feet of the New Red Sandstone is left. At Conijansville about 1/2 the same amount is present. At Cast Valley all of the Heldburyian is gone as the Lower Ovislay only then rests on the Marluries. Out of the sun cracked layer 3C Beds due out Atrypa reticularis, Aspidula galeata a new species (sick). These were in a rolled mass as I drilled into the limestone, i.e. rolled mud ball. It is difficult to understand the various sun- cracked deposits of a limestone nature in the Affek- bachians of a marine nature. We see them almost in all the formations and especially in the magnesian deposits. Certain it is that all the limestones seen are of very shallow origin for one sees these sun cracked limestones (usually in some) emerging into normal marine deposits reflect onto frosts.

July 21 Sunday, Cumberland, Today matters easy in the morning our Startlyp's Meeting. In the afternoon strolled to the southwest to see the 'Twisted Rocks', the annual folded bits of the Niagara. Collected a number of pieces of limestone of different layers from the lower half of the Niagara reptile and Osteocodae. Once one sees these forms the more one is impressed that the Niagarans belong to a distinct fauna from this of Ledy at all the interior region. In the evening Schwartz, O'Hearn and Maynard called. July 22 Monday. Cumberland Spent the day in the Cielings cuts on the Western Maryland between Pratt Branch and Spring Cape. Sand pockets with fossils are not very abundant. In the afternoon strolled at a large one found some time ago by Hartly which yielded many fossils among them entire Edriostracus secundus, a new Rhodo- crinus, and three with recurved arms. The calici-fication is coarse but otherwise the fossils are good. Also some large and entire Spirofer intermedius.

July 23, Tuesday, Cumberland, Potto = Potomac section, Maryland. Took the 7 o'clock train for Mrs. King in the B & O. - the lower magnesian - Just at the station we see an iron ore bed of the Clinton which has a thickness of about 10 feet; about one half good iron ore. Beneath is a shale zone of about 4 feet when another ferric iron appears but not a good ore. This zone has a thickness of about 7 feet. Some shale follows. Note how. The iron ore bed has an abundance of Amphibolites and Orthoceras and some Pectycypids. Also many fugeris. In places an abundance of fugeris. These ore beds are not due to subsequent concentration as the ore beds are inter- mittent with shale zones, and sandstone, and are repeat- beds of a transitional character for shales to be beds and iron sands are a return again to shale normal sea. Many of the more heavy beds are cross folded, Passing over a little hollow one comes to the cement mill and continuing southward along the B & O. To more Clinton. The Clinton is separated from the higher Micgiana by double sandstone, the lower one about 2 feet thick, followed by shales and sandstone about 3 feet, and another sandstone about 18 miles thick, other than the sandstone The Clinton fades without change into the higher Michigan and beneath these sandstones about 3 of feet the beds are red and black - same color.

The Niagaran (higher) series is much thinner at our faultier ferry in the canal, a shale series with thin bands of limestone (2 to 6" thick). The Dolina series should begin with a sandstone 8 feet thick. Otherwise as my section, All of the [illegible] series is decidedly sun-cracked [Ricks has a photo]. These are plain visible up to the top of the fault covered well. They are seen again at various levels up to the decided thin red clay limestone of the upper Dolina. In fact the entire Lower Dolina at different horizons sun cracked but especially the lower half with the cement gone. The Upper Dolina as I left you girls but find found and saw nothing Today to add to the former collection. Passing around the cut and up the Brinckston Rural one comes abreast upon the Cladozona rectilincata beds, of the Marlinos. Higher up, just half 35 feet, appear the coral beds with Farnitis Echinoforina au Bryozoa, just as the same beds as those seen at Carl Valley. Still some higher for 10 to 20 feet appear bed with Placipora ramux- cens, Reusselaria, Hederella, Philidopsis and Ostreocoda. A little farther on saw some bone chalk.

looking like that of the New Redland. It does not seem possible that the green can be here for the jellor (mattures) chalk of the Lower Crisllany som is seen on the road up the hills. A little further down the hill is a coal-metal quarry indicating the presence of the lower sandstones. The entire thick- ess of the Crisllany here can not be much over 105 feet for the Romney is seen a little further on in the road. Salina according to Me is 1080 Nicaraguan .. .. .. .. .. 345 Make these corrections in my pamphlet. The Salina series is first overlaid and then over- be even better for purposes of returning syndics turns about by 10 degrees. On the Princeton road it seems to, July 24, Wednesday, Cementland. Regan Regim. Lot of at 21st Bridge and examined the section on the other side of the Pittomne in Rock No. Saw nothing to add to my former work. Collected a few rocks for the whole horizon above the macro- flumia limestone. We remeasured the Crisllany and found the Lower Crisllany to have the thickness as former guess i.e. 90 feet. The Upper Crisllany lower can not be

more than 160 feet as at the end of the cut off the Romney shales. My printed statement of 284 ft. West Upper Orestay Romney 160' Cherty Zone, Cristkay = 90' R.R. macropleura shale, macropleura division. 44' 20' Secured but little from the Italians in the S.x.O. R.R. hall of guano's. On the dumps collected ammonia fossils from various horizons but in the area for the Middle Cretaceous gone, the horizon with Tectona- lits gyrocanthus. Reeds measured the beds in the quarry and found the shale gone beneath the Lower Orestay 16 feet thick or 27 feet less than at 2/3 Bridge. The cherty limestones with macropleura are 17' 6" thick, the upper then feet being transitional in that they are then limestone separated by shale. The higher shales are clenny pure limestones. There seems therefore to be form for eroded out here more than or 21/3 Bridge. The macropleura cherty limestones contain many round into others than cherty limestones but these have

Lower section at Leizer, Va. (doc.93) September 8-1908. Base. Thin lidded dark hue oratuline. Beds vary 2 inches thick other throughout. About 18' A similar zone with shale beds at top and bottom, but about 1' thick. Central dark hue li. in beds 2"-8" About 20' Dark hue oratuline in beds 6"-24" About 18' Shale zone " 4'-5' Dark hue oratuline in beds 2"-24" Becomes less pure below, passes almost into a magnesium shale. Horizon of Judge Albert R. Camellona across the hills. About 130'-135' End of Lower quarry. At the base of this quarry a small fauna reminding of the East Valley fauna. Phynchmella refleja type, R. Camellona, Bygga, Rhynchospira, Ostracoda. Starts this fauna from this quarry. It is about 100 feet to the base of the large quarry higher in section and of which a section has been published. Lee Hanging Rock section at Papacomo Va. at end of this book.

and into other than study limitations but these have

no macula here then New Zealand fish. These chalk beds then come far away to bear hidden claw crystalline and crinoid limestone of the Cre- crows. Balance of section measured by Reeds but I did not take them down because the detail is not not so readily determinable as some places ap- pear I did the work for the entire quarry. At Twenty Pink Bridge the lower limestone has of the macula gone as in the Keizer quarries does not have this form. In both places the shale immediately above belongs to the New Zealand. The Lower Lias clay that comes in sharply and distinctly there is no transition gone.

July 25 Thursday, Cumberland, Packed our collections (four boxes) and with the one shipped here from Martinsburg have 5 to go to Chm. Haren. Left Gordons at 10 P.M. to get. Queen City Hotel so that are may get up at 4.30 A.M. without disturbing them. 2939 ↓ [E5622] July 26 Friday, To Cincinnati: Started away in a train for Cincinnati on the 5.12 A.M. At Clarkstown & Va one mile out of the Ohio and we have the hilly country of the upper Ohio drainage. The strata appear horizontal and we are in the oil and gas regions. Arrived at Cincinnati about 6 o'clock. July 27- 28, Cincinnati. [Jul 27] With my folks. Saturday with Reds in the morning at the Ludlow iron quarries. In the afternoon on the hill tops about Cincinnati University. [C0520] + C9218

2939 July 29 Monday, North Vernon, Ind. Left Cincinnati and the C. & O. at 8.20. At North Vernon we were late 20 minutes and missed connection for Madison. Had to await until 5.18 p.m. Just east of North Vernon may be seen the Rock Ohio shale again or mere Hackle shale free of the latter type, gray flinty, crumplyrite. One mile east of the station in a small stream valley may be seen the Hamilton magnesian limestone about 16 feet thick holding Mucropermia media, S. novii, Trochidiptera aciniformis, Shepherdina concava, O. perplanus, Phacops Parretus etc. The fossils are by no means abundant. art. The peculiar feature of these beds are their decided dolomitic character and that the limestones are distinctly saw crocket. The limestone beds are decidedly so and about 8 feet may be regarded as saw crocked. My two points are in those layers. The upper six feet are apparently not seen crocked have one foot with bands of chert hiding the points mentioned above. On the west side of the stream the beds continue for at least 12 feet down so that the Devonian is here at least 28 feet thick. These lower layers are more dolomitie - finely crystalline.

"D4683 Going south-east for 3 miles along the Madison railroad one first encounters the Ohio Shale shale and then at least 75 feet of Devonian limestone down to the streambed. Along the track one sees much widma of very crocted magnesium limestone. The beds or distiguishes are the silten limestones in large bks. The openings of the croctls are from 1/4 to 1/2 incht. The joints from 4 to 8 inches. In going to Madison we again saw the Ohio shale about 4-5 miles south-east and again a little further along. In those places it seems to reprove on the Silajaran.. If this is or the rule of silo indicates an erosional unconformity, The Devonian rocks are in a very uncrm county. But once on the Silajaran rocks the county is again flat and remains so almost to North Orkadian at the edge of the cliff to the river level. Staying at the Madison Hotel. C9222

July 30 - Tuesday, Madison. The section at North Madison down the hill to Madison is as follows (on P.C.C., & H.L.P.R.): Heavy bedded Niagara dolomites with casts of Crinifera radiata, Atypa reticularis and others. Chunks after first level county. Seen 10 to 20 feet. Then bedded Niagara dolomites, almost shale in places with Phacocaylke romingeri (that globular heads), Calymene micranensis, Atypa reticularis 10 or 12 feet. (See 2-5 inches). Conformably follows passing into shale (then bedded) chalk and probably magnesian. About 10 feet, no fossils. Heavy bedded dolomitic limestone with here (corrugated) (looks like sandstone) are there a thin shale parting. It one of these collected to the lot packed. Oryzora, Defendita (? coecifera), Amblychir and Orthos senectus. Orthoceras common 25 feet. The fossils are few within 3 feet of the top. Followed by the same kind of rock but thinner bedded (3-6 inches). Upper 8 feet with some of the regular Richmond fossils. The lower 2' almost a reef of Calaprocera Faristella stiletta and some Tetradium, 10 feet. More thin beds of the same nature in them and thick beds with few fossils. About 8 feet. Then the thin bedded limestones and shales.

"the regultion Ohio Richmond beds only Rhynchotrema capax. These beds are seen in two cuts representing a thickness probably of not less than 150 feet. As far as this section goes lithologically, all appears to be conformable as an unbroken sequence. The last of the Richmond becomes mag- nesian, lighter colored and seems to shade over into the Silurian. However the lower Richmond beds already give way to shales in which Corbulus arphoid. There are no transition beds to these shales and yet all appears to be a sequence. Immediately above the thin dolomites have underlaid higher Kicjaran beds of the interin type. Purchased 4 photos showing the outcrops in the R. R. cut and the staging tracks. Left at 2:15 for Battle Ground and due at 4 for Louisville.

July 31 Wednesday Louisville Ky. Just visited the cement quarries at Portland in West Louisville. Here the top rock is cherty and gristly, forming amy which chars, yardellanus is most abundant. These layers are about 4 to 5 feet thick. The Cement layers are close beneath immediately below. While we did not see the Ohio shale yet the Hamilton shipp's presence in the Huec or clade surface. Here the Niagara quarries about Crescent Junction maybe seen contact between the Louisville Niagara and the Onondaga. The top after a quarter mile distance of the Niagara is full of crags following the Onondoga coral reef. In the latter are for me more crags, such as Michelinae, Spirifer separatus to Spirifer acuminata, Pholthe-nta cinctum and I demissa come in about 80 ft far higher. This is a remarkable phenomenon to see the Niagara limestone conformably followed by the Onondoga limestone. A limestone coral reef or another coral reef conforms so that the eye does not detect the hiatus of the Kealiff, Doline, Heldebury and Clifton any between the two. This art after that one sees such discordances in limestone. The Niagara top is for me Jeros - Delicifits, Halysite, Eriddphyllum, Sturmetone, Chardona

Igellia, Jophrenti, Anastaphia, Cetrypa are Valmanella. Stopping also good hotel the Louisville Hotel $2.50 per day. A better one near by "The Old Inn". Left at 3 P.M. in Clarksville, Tenn. The railroad first goes over the Georgian plains and then through the low but rough hills of the Ohio Valley. The a long ascent into the Mississippian Strata. At Elginville Town we are in the St. Louis and remain in it up to at least Darling Green by a distance of 70 miles. Through this country one sees small holes and but few rivers. The climax of holes is about the Mammoth cave Junction (there is 5 miles to the west). The county is constantly of ad down and but few of the hills have ponds of water. The limestone is deeply dissected, the red earth is deep as the fields are covered with it so that stone walls are made of them. Arrived at Clarksville at 9.30. Staying at the Tulane. Cost especially good at $2.50 per day.

August 1 Thursday: Hartville. Spent the morning on the hill to the east of Reesor- n's Hill, there met the many small sparse quasimopodus megalos for hand anted. Near that occur the greater abundance of Orthoryn- chulus linnegus, Orthus sinuata, O. Aculis, Plagi. Styphla crean laticostata Rappogquinia. This same is about five for thick. Then the beds about one for thick hold Archilena. Lower on the same hill to the north, about 20 for lower, are the Tetractuni hus. Here also occur Orthorynchulus, Latexhia at naval a Clammaria alveolata. In other detail see my note book of some years ago. In the afternoon to Marglis Hill east of Reesum Hill. Both Hills have the same section and the strata dip quite perceptibly to the S.D. At the top of the hill in the old fortifications occur the bygora hus of which I collected. Besides the bygora and Orthoryn- chulus I collected a Phyllaprina, Ceramurus flumexan- threnus, Lickas, and Calymene. If these beds are topmost Trenton it is curious that one does not find Tremmelensis. Why are only these hus equivalent of the Utica, the southern representative of the Utica.

Aug. 2, Friday. Keowson, Tenn. Told the 7 A.M. train Chattanooga, Nashville and St. L., for Keowson about 16 miles east of Nashville. Then walked 3 miles west on the track to the most western quarry open for ballast. Here maybe see the following section. Fullers quarry. Chirp Rock shale This shale is much thicker in the adjacent hills. Transition shudden. <healt> Omni li. About 4 ft. du Forte for the dawn a Shag bedded. <healt> No apparent healt. Louisville then bedded limestone with occasional one shale. A very hard limestone. No cores seen about 20 futs. at top as at Louisville. shale 2 ft. li. 1 ft. shale 6 inches Shagbedded li 4' Limestone and shale Forte cells. auth, halumin gne bradham shale 4ft.{The horizon from the bradham beds. 11'6" Regular bedded li. for ballast Beds 4

(2016 W. of Fullerton) Periam Section shining Hamilton above Anderson Platy Forsets. See S. J. A., XII, p. 408, fig 1, 2. McCull Hole { 1-2' far away hole mts Baroside = hardly saddle 1-2' heavy water & arenaceous li, Anchycressius bulbosus Tarpi delicta ? Primitive molythen Ceratiths of train about here Crimidol 8' heavy bedded vasself crystalline li. with Anchycressius fauna. Oruley Limestone, Michigan, In conversation with Barde April 1908 August 13 Saturday Dawson Tenn. Took the 7 A.M. train to Dawson. I looked of the abandoned quarry near the station but seemed for less than in the Fellers quarry; Reds worked the Feller quarry but came soon shut in and started all around. Returned at 1:32 P.M. and packed three boxes. The latest batch will ship by

"deemed a poor quantity of Walden crinoids and few shells. The def is to the west and south-west. In the quarries the beds dip at a "20° grade". The Walden fauna is as prolific here as in Indiana and so far as the brachiopods are concerned there appears to be no local species. The only absent form is Rhynchotreta americana. Among the crinoids there are several local (?) forms (Eucalycocrinites) and a ? Cayracrinus quite different from anatus. None of the crinoids are complete all have been broken before centrifuged. Many of large calices lie with the broad tympans side downward on the basal symin some a few miles away. Many of brachiopods are separated shelves. The hybrea are less common here than in Indiana and this is especially true for the Trematis jones. August 3 Saturday. Dawson Tenn. Took the 7 a.m. train at Dawson. I looked at the abandoned quarry near the station but seemed for less than Zacheus Walden any point. Reds worked the Fuller quarry but came some it in and stopped all around. Returned at 1:32 P.M. and loaded three boxes. The later Batu will ship by

freight and mail hit loading to Camden, [2949] August Sunday 4, Camden. Left Nashville on the 2:15 C. G. W. L. for Camden.. Arrived about 5 P.M. More Mijaram to the next station, Popram, only Fillin grams north of Newson. Then through the Black Hole and dance into the Mississippi. 4) August Mondays, Camden Collected in the Camden Lower Christany in the villins about the village to the south. In the afternoon on the hill slope back of the houses in the northern part of the village. Secured one oratured than on my former try. So far as I can see the Christany is followed by a zone of Hueist-red shales without fossils. It certainly is not the Hoell shale. This shale in places terminates in a layer of Haell much with wood certainty of Tertiary or older recent age. Then an injected redish sand indicated wtr an rim zone of 1-2 inch thick of base in contact wth the side a brown coal. All of these deposits are very modern and have nothing to do with the Pelegrines on the Christany!

The Camden has strong dips but did not measure them. Why is it that the zone Devonia appears once on the west side of the Tennessee. August Tuesday 6. Hollidays. Started out with a buggy at 7 A.M. for Hollidays and after driving for more than one hour found that are none on the any road. In driving west, road to Hollidays we came upon the Heldesturjian about 1 1/2 miles to the east of Ellis [illegible] in a small stream bottom. Here we saw a few feet of the top of the Heldesturjian immediately beneath the Camden shale. The former is of the same character as that near Hollidays, mine a thin bedded limestone than shale. These beds are full of byrgon - the Trematostroma beds. The Camden comes in sharply - there being no transition between the two the Camden and the Heldesturjian. (1) About four miles north of Hollidays beside the road we spent the day in the upper beds of the Heldesturjian. Here it is a thin bedded limestone series with shale facies bearing a mass of byrgon. At least 25 feet is shown to the road. [illegible] these beds [illegible], [illegible]

Jculamellona, Anostrophica are Syphidula galenta are seen. In other areas regular New York fossil New Zealand, (2) Below these limestones, to the east of the gravel down to the streams may be seen the shaly series of the New Zealand oolitic orbit: Cetylod reticularis; Rhipidomella Meta, Leptaena chesbricdoli. Also Peripha macrphylla, D. pulamellona, In about the middle of the thickness may be seen now a Camarcocinus payment. This zone is mostly of an 15 fut thick. Below these in the stream may be seen solid crinoidal limestones, the top layers of which have Camarcocinus in abundance and stems of what in New York would be called Mariacoccus (Smith nats). This is underlaid by the same limestone stone known on my former trip at Allens Mills - at the top of this series there is or here collected the species given in the N.J. A.M. How much of this solid limestone is Heldubuyian I can not say. The Camden effect is seen in many places along the roads, at nearly all the rivers enter the bottom lands. And now are three outcrops are meet the their zone of Camden clays formed upwards and by the iron bearing yellowish sands.

August, Tuesday, 7. Perryville. Packed on two boxes and shipped them at Camden. Left at 9:58 A.M., and left for Perryville via Hollow Rock and Lexington. Arrived at 6:30 P.M. after a walk of 4½ hours at Lexington. 2947 August 8, Thursday, Perryville. Was up at 5:30 and away at 6:15 in the quarry near operation about ¾ miles north of the village. Here may be seen the top 20 feet of the Browns-peak upon which rests without apparent break the New Zealand. It begins with a limestone member probably 5 to 8 feet thick, a crinoidal limestone having an abundance of Mariacrinus stenius and an occasional Camarocrinus. These same beds also have the regular New Zealand fauna for in it I saw Stenijus magnificus, S. pelamella, Stricklandia beechi, Meristella atrica, and striatipora. These limestones are followed by blue shales that weather out as a tough sticky clay full of fossils of the New Zealand type. Only one animal comes from these shales, here appear the first Brycidula and Michelinia. Above is a debris of Camden shale mixed with sand at some of the [illegible] Luderburge clay. It in clay.

out for a road metal. Did no work in the afternoon. For hit. 2947 August 9th Friday Oxim Springs. Set up also and was away to Oxim Springs by six o'clock. Here we saw the only blue licks spring and then collected all the morning on two "slades" to the southward of spring. In the upper Branch of the Astracaspargia are common but the other kinds are rare. The lower Brandyport has quite clay well and those in places abound in Astylospargia. Did no work in the afternoon. To which I determined that the summer lack is too much from me and concluded not to go to Oklahoma. Ruks will go to do three orals field work. Paid him the various sums laid out on the trip amounting to $16.00 Also paid him $34.75 cash in account and gave him a check for $115.00. Both of these items are to be accounted for on his trip to the Arbuckles and his return to Sale.

August 10 Saturday. Return to Louisville. Shipped one box from Pensacola. Left at 7 A.M. Arrived at Lexington, 9 A.M., deported thence for Paris where I arrived at 11.30. Left Paris at 5.10 P.M. to arrive at Louisville at 3.10 A.M., when I had a bath in a sleeper and then slept until 6 A.M. August 11 Sunday. Left Louisville at 9 A.M. Arrived at Cincinnati at 1.50. Had dinner at the Grand Union and left on the Big Four at 3 P.M. About 25 miles east of Louisville on the L. & N. the last of the Ohio plain is seen, from the topography is undulating and the higher Richmond appears seen of Madison, Ind. Then entered the land dips constantly into lower Cincinnati beds. Arrived at Cleveland at 8.40. Staying at American Hotel.

'2944' August 12. Monday Sandusky. Left Cleveland at 7 am. In Sandusky 60 miles east of Cleveland. Then with car to lake port to take the steamer across thery to the Peninsula, Landed at Ohlemacher one of the large quarries of the Marble shale here is attacked. These quarries show about 25 to 30 feet ex-panse. The material is largely quarried for lime making are rip-saw material. In the upper layers fossils are most abundant and. You see in the lower layers the most common fossil is Styphnodictus em-caura. Other fossils are A. demissa, S. (small pygmae) Stypia aspera, Chonetes (?) scitula, Stictospora. Of corals there are many Cyathiphyllum carobitum, Farneis cunicus, Eophrentis, Cystiphyllum etc. Two species of Hymatosporea. Concardium and Leprecanus (one about 10 inches in diameter) were seen in Mr. Clemens collection, an old farmer living near Ohlemacher towards Lake Erie. From a quarry man (crane sparta) I purchased 2 Macerpectalichthus sullivanti for $2.50. Will ship by express. William Bird, Lakeside Ohio. From what I saw I am certain that all these beds are of Onondaga age. There is nothing to indicate

of the Hamilton fossils. The lower 10 feet are of heavier beds and apparently more magnesian and less fossiliferous. This is the zone that is desired for lime. The upper 10 feet are of thinner beds - even shale. However no separation can be made at this point for the fossils in both divisions are identical. In places the beds are glaciated and deeply channelled (not so pronounced as at Kelly's Island). The Lakeside quarry seems to be operated by the Kelly's Island Lime Co. These beds carry more brachiopods than the same beds on the south side of the lake at a. Here they are more brachiopod bearing, there coral reefs. While the game corals occur in both places yet they are more abundant in the north. In the north the beds are more cherty and the fossils nearly all siliceous. This the alteration to do with being near a shore or is this alteration due to leaching in the north at points here because of the Black Rock cover? It seemed to me that the Chama cutis are most abundant in the coal layers. They are present in good abundance and especially in the lower 10 feet. They are far removed from land,

-14 Wednesday August 13 Tuesday, Canton, O. Paed the Sandusky Passes and shipped by Express. Left on the B. & O. R. R. for Carth at 11 A.M. to see brother this. Met him well at home with one of his regular bone attacks. Still had a good talk with him. Remained at his home until the next day at 11:30. Returned on the 11.45 B. & O. t. Cleveland, Left the latter place at 2 P.M. and arrived at Niagara Falls at about 9 P.M. Eastern Time. Stopping at Imperial Hotel. August 15 Thursday. Lewiston. Started out along the Central Lines in the hand down the gorge to Lewiston. The Lockford dolomites consist of series of thin and heavy bedded dolomites in which measure the fossil curules (mawigures?) the joint curules and once a len piler with calcite. Otherwise along the bedding planes one sees crinoidal material. The pink heeme [illegible] demand turns the Rochester shale. Towards the base the bearing bed shows a distinct cross bedding - the bottomy shell's water- while higher up the thick beds look more like water limestone but are not

"[illegible]" layer. Beneath the [illegible] bedded layer about about 3 feet thick there were action of some free for the creature is considerable though of course thus Beneath this layer the chalked is already somewhat shaly and written out as a partial shale almost horizontally. Then gneiss about 1 foot thick and then appears the regular Rochester shale, or far as general appearance for almost bare of fossils. The first abundant fossil gneiss in the Rochester basin bedded limestone also only 27 feet to appear about 15 feet pure top. This gneiss goes down through thick and has some thin layer of limestone filled with the characteristic byssina. Then follow beneath a mass of heavy bedded fossiliferous dolomitic limestone about 15 feet thick. Out give gradually to common of the species of Omerolnia glyptodonta large, also on. Then a sheet gneiss about 4 feet thick. Scarcely fossils. Then open up thin out heavy bedded sandstone slightly cross bedded and in places divided about 6 feet. Followed by sandy and red and green cross bedded limestone forming itself into alternating shale at these gaps of sandstone. This the regular Medusa series for Orthophycus laevis appears almost in these thin beds of sandstone. Sometimes the sandstone have this gneiss irregular 1 inch, and here of to 1/8 to 1/4 inch. At other times flat shale wedging up to 2 inches cream. In other places

"the red shales pinch out and give way to the green sandstone. In some cases one sees careful out places filled with sandstones then - This is certainly due to a transverse action cutting not the fine regular beds but later filling in the same. Then one is down about 15 feet beneath the top of the Medin, the alternating beds of shale and sandstone become decidedly irregular and then one begins to meet out comminated Lingula acuminata. In other words the shallower sea becomes filled of transverse layers practical ones within the zone of Continental deposits. These lower beds also do not show any room bedding and more shales prevail than the redded sandstones. Then for about 12 feet below the series just referred to (or 27 feet beneath top of Medina) occur the Pilegypsin collected - the regular Medina species associated with the Lingula. These red Medinina shales continue about 18 feet below or in other words the red shale Medina ends at the top is about 30 feet thick. Then follow a great ammonous limestone affiliated with Helyspar and Defendilina careysiana about 4 feet thick (I got these points before at Stannister on the so-called Clinton then). Then a green tinnite shale with a

for the sandstone near the center, This zone is about 20 foot thick. The heavy bedded sandstone join[s] ten foot thick (Could not see beneath the cliff). Shiz[?] thin. Below are red shales apparently divided from sandstones or hard beds. These seem to go down to the rim and may be over 100 foot thick in the exposure. From the evidence today it seems to me that the Medina is far more closely related to the Miajaran as here shown than to the Richmond Gap area. There is not a single Richmond fossil present in this Medina [illegible] while all seem clearly related to the Miajaran. The upper or prolificuous Medina is clearly a marine deposit for about two-thirds of it is regular bedded, one always sees traces of the Alcipula and at about 27 feet from the top in a zone not more of mud[?] thick is where I collected the pelecypoda. This upper Medina clearly goes over into non- typical marine deposits in which there is much cross bedding, some scouring out of deposits and subsequent filling of the cavities, rolling of mud into irregular pellets and brecciating of shale into the sandstones, and occasionally a little evidence of irregular

sum-crading. It is in these deposits that one finds the Arthrophyus and other so-called peculiar molluscs. Finally the red color leaves these deposits and the next 6 feet or so are a white sandstone. Above these sandstones follows at once a difficult shale - a green shale and then the Clinton clomites. There is hardly any thing about these Clinton bricks to distinguish them from the Rochester shale -- it is only the presence for further things as the Breistonia cylindrica and the Athyris quadriflicata. Can it be that the top of the Medina represents a land interval and that this Clinton is the final a topmost marine invadery from the salt. It is at Rochester that one finds the Pentamerus Maynes in the Clinton but it is not present here in the Glazara River props. Then too it is at the close of the Clinton that one finds the reefs with the oristum species. At the top of the Clinton here there are no reefs and all the forms seen are those of the Rochester. The next highly prolificums zone is near the center of the Rochester shale and in other 20 feet one sees the regular hygonan and associated fauna. Then practically barren shales passing rapidly over into the prolificums dolomite.

"It was greatly unexpected to find beneath Clinton fossils bearing beds and the reptilian Medinina fauna the same hygrozo beds seen by me some years ago at Hamilton and near Washington. These fossils which will certainly pronounce Clinton as it has one of the characteristic Clinton byzoros of this. Further it is from this zone that came the starpike sent me by Grant. Amongst those byzoros I saw a valve of [illegible] and the slope later will indicate the balance of the fauna. If these fossils conclude with the Ohio Clinton then clearly the true Medinina fauna is above and is of Delurian age. August 16 Friday. Lockport. Departure at 8.30 p.m. from Lockport arriving there at 9.00 Called on George T. MacCombe and he took me to the Whitmore quarry. There about 20 feet of Medina is shown. The basal layers are 5-foot gray and white sandstones with little cross bedding. Then follows about 10 feet of then bedded sandstones with some shales. These sandstones are decidedly cross bedded. This forms the top of these then bedded sandstone that Dick Law collected the Medinina fossils. Then come in mostly shales with some thin sandstones over the agyptium convolutions but the irregular ones some of which are oval ripple marked and others

shar plainly the way of a bed, On such a layer maybe seen cross marks of the spiller heaver and here and there a Lingula cerventa is caught part with ails around it. It is remarkable that these layers are or often mean left tide and got some strata to follow in to. About these shells which also have an conglomerate bands of almost lim rock are found more cross bedded sandstones. Probably less than 3 feet thick, see photographs. There was originally more Medina but how much is not determinable at this locality, In the afternoon after the rain visited the Kelly and saw the Rochester shale and later tried to seek contacts between the Clinton and Medina but failed. Mac Crute has a fine series of Stromatites from specimens 3/8 inch long of nearly 4 inches. Lockport is a nice good place to study the Silurian section from the standpoint of the section but is good to collect the faunas.

"August 17 Saturday Hamilton, Ont. At the head of Ferguson Ave on the side of the 'mountain' may be seen two sulphur quarries. The lower face is about 35 feet in the man a blue- shale series helow becoming somewhat red at about (Change to about 6-7 feet thick) 2 feet from top and then green with some thin sandstone are turrets that the dolomite offers. below these become more pronounced in the upper 8 feet and about midway in these 8 feet there is a two foot layer of cretaceous material some of the greens 2 to 3 feet wide. It is out of this upper 8 feet that my fossils came from (later it was seen that the lower dolomites come in here) Upon these Medina deposits follow some blue shales in which the dolomitic thin has become more abundant, and finally these dolomites persist until our shales. In these dolomites at first there are but few flat nodules outside at the top they are very abundant. (5 feet seen) This zone is about 20-30 feet thick. In the dolomites above the blue (? siltstone) shales one sees the regular Niagaran fauna of this region: Orthostre, the large me) Colymene, large head of litho delmours or Brumastus the long eyed Acidaspis (near the head) Dolmanites etc. both gave me this fauna as a The M? In the upper flat nodule horizon is where the forages occurs. See the fauna in the N J.H.M.

In anthogany, a layer one, a few hundred feet to the south one can see the following: At the top the reddish-cherty dolomite used for road metal (has the sponge fauna). About 8 feet thick. This passes gradually into other dolomite in which the flint nodules are [illegible] and broken. Then, as usual, the dolomite highly crystalline, a bluish white, about 8 feet thick. The fossils are those mentioned for the quarry. Below a series of blue shales with bands of dolomite (about 2/3 shale) about 10 feet thick. This is only one of these shales in the thin shale partings in the next series that has furnished all the reptiles discovered by Merian at Keely. [illegible] on many canities filled with calcite crystals Then - one bed of dolomite about 4 1/2 feet thick. Then 3 bits of dolomite 1-4" x 1-6" x 1-8" and slight slabs dolomite gastropods. Then 2 layers each 18" thick. Then one 10 inch layer another 8 inch layer, then about 18 inches of the reddish dolomite, one of which dolomites have some shale between. Then a little shale and then sand to base of quarry. This indicate that the fauna collected by Frank at now - in the N.W.M., is from these lower dolomites. The fossils are one little bivalve with thin pyrite or an oxidized just a rusty yellow. This makes base of quarry. Along the term pit line one sees that a series of green shale with many bands of the bits of [illegible]

Hillum beneath the base of the quarry. These make the th of the Medina. These do not seem to have a greater thickness of more than 10 feet other than the section of the first quarry takes of ad goes down (Bullers) To the south east of the mountain turn piles there is another quarry. When the latter section may be seen in one wall. There as in the other quarry the base is where the dolomite begins all the Medina sandstone still efflores. This face is about 32 feet high, The Medina along the turn piles are not quite close are those at the top of the first visited quarry. The concretions layer is here, but low and dwindled, and about eight feet beneath the gray stone in seen the red soil of the first described section. This for these latter beds that I spot my Medina forms. A little further down the road we see that the dolomite series makes a precipitous cliff while the Medina beneath makes a sloping surface. The Medina red bed gneiss is about 1 to 6 feet thick and about 8 feet beneath the dolomite. Going down the hill to Ferryman Arc one sees that the entire here side is of a red clay just like the old Medina shale beds in the Mojave gyps. From the cliff down of to the dolomite the elevation maybe 200 feet.

but is probably less. Over another Phycus hearklam in large slabs, about 3/4 mile just north by Song not the mountains railroad about 3 miles me has a good exposure of the Medina. Further south the Red Medina as in the Chicago house with whole grit or recessions green sand and John for a mile me has an other exposures. At the turn on the rail road about 3 miles at takes there is a slope of Medina about 35 feet high. Then comes in thin redded red sandy tone alternating dark shales for a thickness of about six feet. Then thin and heavy bedded iron layered sandstone over the whole formation for light This is the same grey as beneath the quarry. Ever clear for about & foot. This is the same that is found the Hellbore and other layers. In the end lies immediately film by the Langelli branch, Lingula cancuta etc then follows closely the town quarry limits. They make their way by cliffs on the Medina, did not go now 1/2 mile further as nothing more could be seen of great exposures. But they'm certain that there is Mr Clinton Mr Ros- chester about Hamilton. The iron Loughs rests directly upon the Medina and apparently the same Medina as at the Chicago page. In going south to Holland one sees the old red lakes almost in the lowest rocks. From Stony Creek to Vinem out one sees the same series as at Hamilton Distance 11 miles from Hamilton. After this there

Boxes shipped 1 p.m Vincenton by Express. Allert. 5 u Cumberland, Md. Freight. 1 u Louisville, Ky. Express 3 " Nashville, Tenn. Freight. 23 " Camden Tenn. u 1 " Perryville, Tenn. " 1 {Cleveland Q. Express {landucky spk's. 1 " Niagara Falls Express. are no expressses an the rail-road is some up the upper plaine that extins to Niagara Falls an Buffalo. The Medina T'J is thugme a land intervale on whil The Clinton an later Dilmerie peas trans passed. The Lorraine is found in loose bordures at Hamilton, thrown off by the lake. At Toronto the Lorraine n upspred. See Parls for the section. August 18. Sunday, Niagara Falls. Seeing the falls today. Will leave on the 7.30 p.m. for New York. Shiffted a trip by express. In the after noon visited the ju arrive N

the Buffalo Cement Co. Took three pictures. The Onondaga rests rather uneasily on the Marlins. There are irregular projections up to 2 feet high and oafs as deep as 4 ft. Corniferan cards may be seen resting directly on the Marlins. The break between the Bertie and Onondaga is marked lithologically for there is no irregular erosion line here. Left Onondaga Ferry at 7.30 A.M. Buffalo 8.35 and should have been at New York at 8 A.M. but did not arrive until 10. This by the Greatest Railway of America! The Porter said this was the regular time to be late. Several local trains shot by us.

&. la. (1) :93

Stanjay Dick section Sep. 9-1908 at Gapacomo Dr. Va. When Cristany. Oreay huddled whitish sandstone with green conglomerate near top. In other parts the Cristany becomes crazy toward the top. Conglomerate goes with marked bed- ding planes. Quartz pebbles chief. Quartz pebbles up to 3/8 inch, rounded. Lower Cristany Distinguished here from Upper by the very bits of chert interlaminate with the thin zones of sandstone. Also more clear interruptions of go-kelly. There is a lamination between the two zones rather abrupt. Lower Cristany in one cliff near north end 1 section about 70 feet high. L.O. more prolific forms than after Platyceras abundant, Estmoia sinplana, Leptocerdie flatellus most common near base Heedenbug. Macropleum- In both places of this and there is a hollow beneath the Lower Crist.

ad above the Macrpleum bed. The cliff above each is 20 and of the other 70. Distance from house to 70 steps or yards. Thickness of the Macrplenum cherty limestone about 30-35 feet. makes a cliff. The fossils are the usual ones: L. macrpleum, L. fademellan, L. cycliptem, L. chm bricoli etc. Whipidomella Gaphritis, Eatma mediola, Steph. kedi These beds I am descending with- out much into Cryman and gradually turn the cherty. The Cryman form leeman modular at first to resemble the Marbles of being less regularly bedded as not the other limestone. The cliffs here show the 30 feet of Macrpleum and at least 25 feet of the Crymans. Beneath the arch and there seem due to the tricks at least 30-40 feet under the the bedded modular Crymans.

3 A little further south the red line higher at the Merlin appears down to the Rhyncho thene known as Byssogher of the D. B. B. section. Shelly gne at south end of cut about 32 yards across, dip at one side being vertical at the other about 50 degrees. Lower Orielay. At south end of section thalff about [illegible] 285 foot high above South Branch. Of this about 260 can be seen. Down the separation of the cliff Lower Orislay in the upper Orielay is merged. Fully 70 feet of L. C. can be seen. This then would make the Upper Orielay 185 foot thick and all of the Orielay about 260 foot thick. What can not be seen is interpreted to be the shog Veludby above the Muerdfum bed. At the south end of section girth behind the Parson house [hotel] may be seen 20 feet more of the roof hidden coarse Upper Orielay or that all the Orielay here overcomes 280 feet. It may even be thicker.

As one goes to the top of the mountains back of the Parnon house the coarse sandstone part times of conglomerates are very noticeable. The pebbles from the ground and some are as large as half an inch. The Central and Gulf continues the entire Diluvian time passing without break into the Marlins. A less topography prevails to the East for the deposits are essentially limestone, though somewhat impure. This is continued into Crymours but towards the close a higher type- topography begins to appear seen in the chalk hills of the higher Crymours. This becomes more decided in the Maers Plains hill and then the sea becomes very muddy and finally on land. The Lower period in the western Cumberland Gulf prevails while in the east was deposited the Oolite and onto the Oolites the route again becomes gravel throughout the Cumberland Gulf. Elevation of the land continuing to the east on the Predmast slope and the Oolites losses more and more of its lime and becomes sandy and fry a conglomeratic sandstone in deposits. Elevation continues and all becomes land.

At Cumberland on the 7th Aug I find they the same cruel warate appear as here. Or the conditions are worse for the Cumberland at Bull.