Field Notebook: Massachusetts, New Hampshire, Vermont 1921

Schuchert, Charles

1921

Yale Peabody Museum of Natural History

Original Source

Source Material:
Image from the Biodiversity Heritage Library. Contributed by Yale Peabody Museum of Natural History. | www.biodiversitylibrary.org

paleontology stratigraphy fossils

Document Pages

72 Pages

No text detected

35- doc.119 Boston - Cambridge -

Boston - Cambridge - Greenfield N.H., - and Vermont with Keith 1921 doc. 119 Charles Shuchert Yale University New Haven Conn. 1921 doc. 119

No text detected

July 22-29-21 Friday New Haven, Conn. Left at 10.32 ad for Boston at 2.15. About 3.30 drives visiting with Raymond. In the evening had dinner with him at the Harvard Club.

July 23-1921 Boston, Mass. Worked all day at Mus. of Comp. Zool., Harvard, picking out duplicate brachiopods of the Delany collection of Bohemia. This a very complete and totally different one than orthids and strophomenids. The Ordovician species are not many and all come out of shales, sandstones and limestone like concretions just out of shale. Saw Dalmanella, Plectorthis-like but appear to have a cruralium, Hetutella, something like Orthos elytra, Triplecia slightly lamellose, Plect ambritis, Rafinesquina and Schizocrania. The whole reminds rather of dip. Trenton. Of Silurian saw nothing of the earliest, a Allemandian fauna. Of middle Silurian the common genera are Dalmanella, Phisida orella, Bradyorim, Strophonella, Schizocant ella, Plectambritis,

I saw nothing to suggest an upper Lurina. Of Marlius (7f) there is of course little but what there is appears to lead direct into the Konieprusian. Of Konieprusian there is a large lot of Chipidomella, Schnuckutella, Shepherdata, Shydmella, Plectantmita?, Orthotheka deforma that come out of Schnuckutella pictura like forms. Chonets, Amplia, Leptotrphla, This fauna is my suggestion from New Zealand. Of the Gc gone there is little and it is not suggestive of Lower Oeornia, rather Middle Oeonian, but upon the whole there is little to from. Of H I saw no backs at all.

July 24-1921, Sunday. Boston, Mass. At ten took the South Shore steamer for Plymouth. It takes about 3¼ hours to go. At Plymouth we has about 2¼ days. Outside of the immediate historic places there's not much to see. The place is living on its history, and even though they should have celebrated last year the 360 anniversary they are now building a new water front and marines.

July 25-1921 Monday Spent the day at Harrow looking at British hackifords of the Helder collection. The Noni[illegible]ssian is the great rarity of the collection and has the finest material. A wonderful array of Dictyrella, [illegible], Merista, Meristella, Eospiina, Altpa, Rhynchopira, and Beachia like form (T. onelonica) While there are forms reminding at once of New Scotland yet upon the whole the fauna is a different one and a subprovince of the Arctic Helderfuran. Anastrophia is native. The hackifords were marked F for thank I think some are from these Hackell limestones. Of G [illegible] in my little, and J H mother. Of the Silurian many forms are suggestive of the Noni[illegible]ssian and for this reason Barance (he) identifies species of the two formations. Most of these if at all will prove to be different species. In the Silurian we see no Partamorus flavus. Rhynchotreta cuneata is here but as

she chenell. a rule the species are again very different for those of the English-Swedish Silurian, and quite different from those of the American Silurian. I saw nothing that is certainly greater than Luelhi or highest Louisiella. Conchidium Knighti is very rare, and some may have to say that said Luelli is present. If so clearly the introduction to the Devonian and Permiferousa. According there is a break here and all of the higher Ludlow is absent including the highest Silurian in the Tonolaway. All of the Ordovician is absent and or Cc may = one Armada after. Of Lower Cambrian there is more. The Paradoxida fauna is once developed. Of Upper Cambrian, Ordovician, Carboniferous and Chazgian there is more. All of the Ordovician appears to be Markations. There is no Cincinnati and apparently no

earlier Liluria = Alexandria. I am getting a fair array of Bohemia hachidraes, and if I should take the time to sort of the unlabeled lots I would get a just deal more. The Schary collection and all of Barande's species should be restudied in the modern [illegible] of the feneric terms. Probably many of Barande's species are of varieties. All in all it would make an interesting study, and many a new genus would turn up among the siphonellids and spirobaceous. Then two contrasts should be made to show the provincial character of the Bohemian fauna. With Barande's fine illustrations and this Schary collec- tion then should be no difficulty in doing them.

July 26 1921. Tuesday Boston Mass. Finished today picking out a duplicate set of Bithemian brachipods out of the Johary Collection. I have picked out about 200 species, and Barrande has described about 600 forms. In the end I doubt if B. has as many as 500 forms. When the Johary collection is wholly labeled, there maybe 300 and not more than 350 forms. The great majority of species are in E2 and especially in F2. Then in D, next C, F1 and least in H. What I have will make a few exceptions illustrate all the genera. I can now Steptoi or Paterula.

July 27 1921. Wednesday, Raymond found more specimens, or I finished selecting to day. We have picked out the following :- Bangkley has Ondorian - 50 - 19 lots - 98 speci Lilican - 250 121 " - 1100 " Ff1 - 15 8 " - 34 " Ff2 - 250 105 " - 725 . C - 20 8 " 41 --- 585-261 " 1998 " When there are restudied in the light? Bangkley volumes I should have from 3/3 to 3/4 of his forms. As then is a good deal of specimens in the formations it must mean that Bangkley has driven the species for fire. In the end there may not be more than 400 species and varieties, so any one thave a fine collection as it will serve most purposes.

July 28 1921 Thursday. Boston, Mass. Packed up my box of brachs, and Raymond will ship it by express, Tried out my ideas about the Brehmin succession with Raymond. He has studied the trilobites and I now dare see the brachs, There is no Lower Cambrian The Middle Cambrian in the regulation me of the Atlantic province th'p the species are different south of the Pontiac barrier than to the north of it. There is no Upper Cambrian. There is no Ordovician. For D, I saw our brachs, but Raymond has trilobites and there he says are clear of the Brehmin. This seemingly means that some of the Canadian or Bedd mantum is present. See in Mr Shaggian

Beef all of D is of Ordovician age leaving with the Black River and apparently belonging with the Lister Trenton. There is no Eden or Mayville. The equivalent Richmond is present within a fauna wholly unlike those of America. It is the time and fauna of the Brachipodum Tainiolites Schizus of Sweden, and in a way of the Brachidium of Estland. Of earlier Silurian, the American Alexandria series then appears to be none. So far as I can see all of E is of the time of the American middle Silurian = Clinton - Swellth. As Conchidium Knighti is present in Bohemia it may be that a little of the Dolina is present, but in general it appears to me that all is middle Silurian. There is no Cagnano. The lower Devonian starts in with the Black Limestones of F.1 and then go into the gray limestones of F.f 2. These are the equivalents from Franklin, Creyman, New England and perhaps the Beercofts.

Here is Mr Orlikan. Jno & in Middle Devonian and forms on Amboy. What it represents I do not know. Tomorrow Laf Raymond and I start for Greenfield, N. Henshaw to see Keith: The distance is 68 miles and we go by his car. Raymond returns in the late after- noon and I remain over. Thursday Raymond start next week on at least a six weeks trip to Va., Tenn. and Alabama. This means that T. will not get to Nashville before Sept. 10 and it probably won't be later. He is then to visit Miller at Lexington, Penre- man and Bucher at Cincinnati, and Frost at Dayton. Then Bryant at Buffalo, and finally J.M. Clarke and

Ruedemann at Libby. After this he returns to Harvard to label his material and then comes to Yale to take of the methods of Paleography. I don't if I will see him before the middle of October. This only give me a good chance to read my Text-Book. July 29-1921 Friday Greenfield, N. Hampshire. Started away with Raymond & his car from the Lennox Hotel at 7.30. this fine country and the scenery becomes more mountainous as we go. We go through Lawell, Ashland to Greenfield. Keith's house is about 2 miles west upon the mountain side. From his grounds we have a fine view to the north to Mt Monadnock.

Raymond asked Keith much about the food localities about Knoxville, Tenn. He left after 4 o'clock in a showy after- noon. July 30, 1921 Saturday Greenfield, Mass. A showy cool day with very little of the heat - o:tr. Nevertheless having a good and restful time with the Keiths. Mr. Keith's cousin Mrs Parshley of Gloucester, Mass., came up for a visit on Sunday. Reading Lansing's book on the League of Nations. A fine book and a grand ex- position of the folly of the politician diadem. If he was a lawyer one could not have an international League and court drow away with end of the future wars.

July 31, 1951. Sunday. A cloudy Sunday. Reading most of the morning while the Keiths at church. Much embroilment during afternoon and evening. In the late afternoon took a little walk with Keith to see the sea of mountains to the north of Crumacrell. It is the result of the Appalachian orogeny and the erosion since. Crumacrell rests on an elevated plain between 1200-1300 feet, a plain with others below that front to the sea to the south. To the north rise the hills all out of one Hemisphere. Dr. Gerald Keith Hutton believes that the orogeny's are due to the Appalachian oro-gen-y, buts also believes that there is some late Devonian uplifts. The region about Greenfield is in the main a maul metamorphosed gneissic - a schist - intruded by much porphyritic granite. It may be that all of N.H.'s now and old eroded by early Paleozoic strata. In Maine it seems most of the state.

was around by slates - like the Beede slate of Dater ville Maine. All of this possibility leads leading into to see if any paleography needs wider rectification. The Logan fault may be as much as 40 miles in western Vermont. The basal formation is either a gray quartzite or the red sandstone formerly thought to be the one of the Ordovica. It then follows greywackes with limestone conglomerates and limestones. The thickness is probably not nearly so thick as Walcott states, but so far Keith does not determined it. East of the Logan fault there is another faults? Late Trecassic time, and farther east another one of the Appalachian type. The Paleogries not up on lofty attend meta- morphosed sedimentaries, slates, sandstones are lie, of Algonkian age and older older Laurentian. Keith evidently does not believe there is an Ordovician system. He thinks all is Beekmantown.

In the north the Beekmantown is usually an Archey, Torr. and Ala. It is very shaly, and it is the difference that has led Ulrich to conclude that it is before an older series. Stone, Banks, and Butts are the three great upheavals of Ulrich's Argentine. It appears that Ulrich has not by taken up at the top one member of the Argentine but has as much done so at the bottom. The largest sequence and the most prolificous are as of the Argentine much in sandstone in Ala. and now described by Butts in Torr. Ala. Follies. Under these circum- stances, it can be best to place all of the Argentine with the Beekmantown as one system in the Ordovician. The only our hemisphere have the Appala- Chian trend and ascending ones lie in the App. forecline. See about this paleography.

August 1 - 1921 Monday. Greenfield, N. H. In the morning first crested a lot of female crickets that were laying great nests of eggs. Then autoed to Greenfield, and from there to Peterboro to get some supplies for Keith's auto. Had five rains of Monadnock and Paed Monadnock. To-morrow mean to go from Greenfield to Peter- boro - Marlboro - Keene. Then north over to Westmore- land - Walpole, across the Conn. R. to Bellows Falls -Rochingham, Chester, Danbets, Proctorsville, Lud- low, Summit, East Wallingford, Cuttingville, East Clarendon, North Clarendon, Rutland. The distance will be nearly 90 miles.

August 2 - 1921. Tuesday. Erwin Keith is not ready to go west to Rutland, or must be another day. When he comes east this. Apparently all in order to start to morrow August 3 - 1921. Wednesday. One of the finest of sunny mornings and at 11:15 A.M. are off for Rutland, Vt. Left Greenfield (2 miles) at 11:40 and got to Petetbro (7 1/2 miles) at noon. A few miles further and one more point where had a juncture. This we had agained at Burlin 3 times and it was 3 P.M. when we started again. All the rest were. Got to Keene, N.H. at 3:40 P.M., Walpole at 5 P.M. and Ludlowe at 7 P.M. where we are staying over night. Between Petetbro and Burlin had the first clear view of Monadnock. The road has turns around a large lake where there are many pine

Lomes. Pumphelly has a home due. Between Dalepole and Bellor Falls are less many ruin tenaces and specially on the north side of the Corn. Rion. Ludlow is on the eastern side of the Green Onts, and here towards Bellow Falls the clay Palaeo- grie slate's are altered to garnet ifrom schist. The intended grains that caused this alteration are alsof adjacent. Mr proof are known here but in some of the Huel slates such might be found. These slats are not regionally metamorphic. The Green Onts proper are made of a dome- Hende schists of Alfordian age. A short distance beyond Bellon Falls we left the Corn. Valley and went up the Blackell Rion. Here also are seen ruin tenaces. Ludlow is in the Mack Rion valley. Travelled yesterday about 50 miles.

August 4-1921. Thursday. Left up at 6 and about 8 one are off for Ruthland. Dre for a short distance up the Black River and then leave it. At Summit one are in the care of the Green Mts and all the rocks are Archean,-- granites, horn- or is it Partergne and schist, then quartzite and dolomites. Leaving Ludlow we see some quartzite and phyllites. As we get through the Green Mts I learn that the Archean is adjoined to the rocks over the Cambro- Ordovician series. Then the mile rally of dolomites and Cambrian quartzite, to the east of which are the modern equivalent of the Taomic Mts. Their eastern facies is of Lower Cambrian greenish gray quartzite said to be several hundred feet thick. They too are pushed to the north and underlie the Ordovician. In the rally lies a normal fault of Triassic time. We got to Ruthland at 9 A.M. and as the car does not smell well one put in for repairs and must not start out until after lunch. At 1:30 are are off for West Ruthland to see a little of the great marble quarries. The limestone that lies to the south and from is lost; rully lie in a syncline> (practically all the quarries are in

one line on one side of the small valley. The quartz matt. extend for about 2 miles, according to Keilts inter- pretation the total thickness of the limestones are not much more than 300 feet. To me the thickness seemed great. The limestones are from pure white to more less banded, and very granitic. These gradually give way to dark blue impure limestones, and finally then is again pure white limestones. Every now and then there are thin zones of dolomite, from a few inches to about two feet. The limestones show much flow structure, and this is best seen about the dolomite layers. The dolomite does not flow so readily as the limestone but breaks up in pieces and it is around there that the limestone flows. All manner of li. are much jumbled around and about, and all is recrystallized. It in steepness of the layer forms and seemingly only the faster formed that still show traces of themselves.

On the top near the school where one sees on occasional gastropod. The flavour of these appear to be Raphistoma about one inch or a little more in diameter. Associated with these appear to be Maculina but none seen above more than two inches across. Pured some crystalline lumps that struck to make out to be Rhynchotrema but could not do so, saw no cephalopods at all. May have been some hygro-gra and tiny echinoderm columnals. Are the next to the small flat and mud quarries a little to the west and here above on the side of the cliff the quarries is a grey mass 5 feet thick filled with a great quantity of small Raphistoma ranging from 1/2 to 3/4 inch across. In section these looked to me like this. Here also crinoid-like columnals are present, but saw no plates. Keith says he has Maculina 4 inches across near the school above the big quarries. In one place I thought I could make out in several layers a great quantity of Bathurstia little intertwining. Then started on to Castleton.

Put up at 'The Maples' at Castleton, at $3.00 per day. As there are no granitic injections near the Ruskland area, about 30 miles (see p. distance) the intense metamorphism is due to regional deformation. If Doleritt's estimates of the thickness of the Cambrian is correct the load of the Paleogries may have been 3 miles thick, but finally much less. Leith thinks that the evidence points to deformation during the Appalachian orogeny, and that the mass a mile or more thick was shoved over the Ruskland area helping to cause further meta- morphism. Since then the core has been worn away revealing the intense metamorphism. Then too it is clear that the attraction increases from east to west. In the Bird Lines at Taconics the Lower Cambrian quartzites are thicker, 600 feet a mile, they thin out and in Conn. are only a few feet thick. Their greater mass as erosion intrudes

the over thiny to the east, The L.C. shne therfor lay to the west and the question arise did this sea extend directly across the intervening area all the way to Britain and beyond to what is now the ocean? If this is or, that is, if there was rula of Poseidon, then the Appalachia fissuraline did not arise until the close of Lower Cambrian time. In Vermont it may be that the Red group called Shelburne sandstone, is the direct equivalent of the White quartzite to the south. In the Green Mountains and to the east those directly, the Archean, In the Rutland rally after the Archean comes low join more of white quartzite that gradually goes into a dolomite series of consider- able thickness. What relation these bear to the and of Lower Cambrian ge over the next day purple-free shale series I do not know. In northern Vermont the red sand rock is supposed to be younger than the white quartzite, The red sand rock goes on into a dolomite series at the same time the Third Lower Cambrian Benjamin slate.

August 5-1921, Friday. Spent the entire day along the western side of Lake Bomoseen which is west of Castleton several miles. This is in the slate belt and many quarries one seen taking out purple and green slates. The slate belt gone is probably not wider than 50 feet though in places probably as much as 100 feet has been quarried out. Some days later we saw in the bend of a river that they slate are of the same age. Just above the purple and green quarried slate is a zone about 10- feet thick of slate interledded with thin limestone that range from one to four inch thick. These are always much further apart and jointed into the shales; they are always jointed in many directions and the joints filled with crystalline calcite. These limestones have Loran Cambrian fossils, and still for what maybe Eordiscus (specimens) and I for a form Orstella orana. If these are what they appear to be the age of the rocks is undoubtedly Loran Cambrian,

These joints were sitting at the north end of Lake Bromsen or Dark Castleton. Beneath the quarry gone there are thin joints of dolomite. One of these is two feet thick and is said to have a wide distribution. At the north end of Lake Glenn we saw a joint 6 feet thick of snow white quartzite. Also much jointed and filled with quartz veins. At one place at the south end of Lake Glenn we saw a vertical cliff, a joint striking cleav[?] a synclinal. All was sharply cleaned at an low angle to the east. From this it is held by Dale that the Lake Bromsen areas all lie in I think on it appeared to be a zone of joints all trending to the S.S.E. and lying a syncline. The main quarry gone along north side of Bromsen is of one kind white thro[ ugh] of Lake Glenn are of the other. Probably all the thin limestones and dolomites have more or less of sand, usually fine but sometimes coarse well rounded grains. What we saw today of the Lower Cambrian would not make a thickness of 1000 feet, but are crowded along the strike, not across it.

Schistosity is so thoroughly developed that it has destroyed in the rocks what joints there were. Even the limitations of dimensions and size the quartz veins are somewhat schistose. The foothills are pulled apart and the joints filled with calcite or quartz. It is in these narrow margins that one gets a few joints. A short day of crawling would probably yield a half dozen specimens, and these would determine the value. The joints are of good for time values. Mr. Drinmontan J Harvard was with us all day. He has an area 6 x 4 miles granted in for a disputation. He is after the structure and not the joints, [Comparing this valley with the Georgia one there are seen great differences in the sediment. Here quartzites prevail while that Georgia dolomites of several types and varieties are at hand along with a good development of conglomerate. In both areas, however, Late Cambrian bones occur.] August 6 1908.

August 6 1921. Saturday. Keith, Drinnerton and I first went west tr one-half mile east of Fair Haven. Here we found well exposed the 15 foot zone of thin bedded limestone. I bored a reel continuously for two days and got but a single very small Lingulella a Artied. Otherwise saw no fossils. We than went along the western side of Lake Bomroeen to other slate quarries and finally high up on the ridge at Cedar Point in a slate quarry saw an outturned and cleaved fold about as follows. Then left Lake Bomroeen and crossed over to Lake Glenn and near the south shore found black slate interbedded with but little crumpled this in th- place of the wrong kind. Only seen on August 17th slate limestone. These had every now and then fragments of Olenellus and finally got an identifi- cable piece of the plothella. Here is now modernths

"that all the slates that we have seen today and yesterday are of Lower Cambrian age. We have now seen about 2000 feet of Lower Cambrian slates, and Keith says the whole seam is about 3500 feet thick. A light green but an intense ore, and a grey-green color make up the bulk of the slates. Thin limestones are interspersed near white quartzites, usually thin - from a half inch to two or three inches thick - but at times considerably ticker. Limestones are much rarer and come in guns. One gun of them reddish limestone is about 15 feet thick, and a Hard Shale gun has then reddish limestones less crumpled. For thickness this Hard Shale is later on than Of purplish and red slates there are at least three; one is about 20 - 30 feet thick, and of the other one I do not know. the thickness. The scarcity of the fossils is rather striking and is hard to explain. They may be more common than appears, due to the crumpled ``` ```nature of the lamination of the red and purplish ```

nature of the directions. What is the cause of the red and purplish scales? When red scales are in contact with water give by an intense green. In a condition of deposition, and in one place I saw green slate terminated by thin quartzite (1/4 inch thick) and at once above it red plate. Of course mud bottoms are not the home of an abundance of life. Can these red scales have any thing to do with shallow water or some conditions? I am of the thicken quartzite gives rise to a slate scale marked with oozing, circular in nature or worm burrows. Juveniles there were originally holes in the pastry muds and are now filled with the fine sand as casts was fastened to the bottom of the quartz- ite layer. The quartzites are variously of very fine sand, and seemingly always of clean white quartz sands. The phenomena are for deep water and far away from the shore, or for dry rivers bringing only clean marked fine sands.

August 7, 1921. Sunday. Started north to the east of Lake Bomo- to see the area more less studied by Brinckman. We again were in the slate belt of the Lower Cambrian. It is the succession we saw but along the south shore of Lake Glenn. Finally near Twin Lake we came upon a good development of the limestone, and in it I saw considerable pre- servatory stuff - trilobites - of the Lower Cambrian. Have a few pieces but initially the debris cannot be determined. Fragments of (Clenelles) . Pitopogin spicula are common. Associated with these limestones are flued slate, some of which are marked and those that might be mistaken for gneptro lites. None are, however. We saw the same kind closely along the south shore of Lake Glenn. Near Twin Lake we saw dick up on the mountain side a quartzite lump, about 35 feet thick folded some thing like this:-

"Ballace's Lodge" fore shale. quartzite, white 3rd thick. At another place we saw the basal layer of a thin quartzite among low the shale were thrust into the shale. It was about hith this: are of these folds in about 2 feet <division of movement. Some of the large purple shale quarries, Mr. Jones, we saw a face of more than 100 foot of purple shales, and yet 20 foot is the thickness. We soon saw the cause -folding, closed anticline leading north and sherry of the dip slope = to the west. strike < north dip E. The slates are so much folded that it is only in the quartzite that we can see what actually happened.

"Learning Tarrin Lalle and Irminutim are started most and in Jamin, Huttartom are jarred through the same Cambrian suc- cession. Reiff says the terrains have the same exact succession. At four miles south of Ludbury are come upon great fields of limestone, said to be of Trenton age. These limestone are wonderfully drawn out and kept of like angry state. The hills seem more a fur segment rather opened for the Granod Eleemos. Have two samples of these drawn out limestone. Reiff collected at another place some hack shits that which announces Middle Trenton. From here north are remain in the Ordovician, and it is but at an infolded one which was thrust to the Lower Cambrian seen to the south during the last three days. Ruffland is another fault of these younger strata but have their position in due to normal faulting. At Ludbury can be seen a complete section out of of the Trenton, but finer

"if the Chagy mantles like that of Rutland but beneath the latter, occurs the heavily bedded dolomites and sandstones of the Beech mountains. In places there are said to be in the Potsdam Crin- bedded sandstone. All of this area was once covered by the northwestal arms of the Lake Champlain. North of Sudbury, the country soon becomes a fine farm country, because in all the fine places, the land was covered by the Champlain sea, and the Champlain Clays smear out the ground and make good but sticky farm lands. The first farm yet seen and found in the afternoon lotus of Hyde France started in 1671, is one of the most southern of these places. Set to Middle bury at 6 P.M. and som after, I begin to rain. Here an entirely smooth face of Ordovician limestone north of Sudbury. The Taconic Range goes as far north as Sudbury.

August 8-1931. Monday. It rained considerable last night. This morning it is clear and cool. To the east of Middlebury here in Beekmantown and associated are merchantable marbles. Same occurs to the south of Middlebury. Farther north occurs the Ludlow Trenton, and some miles still farther north are the high ridges of the Vermont red sand rock. It comes out far beneath the above mentioned Ordovician. All these masses are thrusts to be contrasted to the east. The western face of the Green Mts are here lined with a white L.C. quartzite. In going south they pass beneath the L.C dolomites, and higher come in the Hp.C dolomite/marbles. The following is the sequence of the Lower C. from Middlebury south to Mass. At base the Proterozoic slates, limestone, greywackes and schists, White cleaf orbed quartzite 3-100' in Conn. Uphere tr 600'-500 feet. Grey dolomite, 1000 at Rutland. Also li.

"Upper Cambrian\nGreen Sand drl. and quartzite. 400'-500'\nGrey dr. at white ooliterams sandstones. 300'\nGrey fine drl. 150'. Elk Oil, a Cambric.\nMarble shales. 300'\nLimestone consolidated and harden. Little to 400 ft.\nStructural break\nBlack Shale intruded with liq of Ord. area.\nThe Great Rutland marble series.\n\nThe place of the Red Vermont quartzite in N. Mass,\nI fancy upwards for a red or other dolomite 0-100 feet thickly.\nIn going north from Middlebury to Burlington\nare seen in the cross dip ridges that are made of\nof the Red Vermont quartzites. In the Shelburne\nregion they make the shores of Lake Champlain.\nIn Burlington at the falls of the Mississipi River\nthe red quartzites fan gradually into the red\nHitchcock Mississippian marbles and dolomite. Over these\nlies a great thickness of grey dolomites, all of\nwhich are thought to be of Lower Cambrian age.\nAll of those Lower Cambrian masses are con-\nstructed upon the fat little alluvial Ordovician\nseries along the shore of Lake Champlain. To\nthe east some distance but is a great fault.

of the normal type listing the L.C. series down. To the darkward I this fault comes in the [illegible] type Ordovician series but all are much altered and drawn out, and practically no forms can be had. What is the position of the Vermont Red quartzite and the succeeding dolomites? Is it a western phase of the eastern white quartzite? If not are they the eastern phase of the Potsdam and the succeeding Little Falls dolomites? No! What is the relation of the redning slate series of the Lower Cambrian to the white quartzite and the dolomites of the known basal L.C.? Keith does not yet have the field relations determined and as yet has nowhere seen contact to demonstrate the age relations, The basal white quartzite are clear washed fine sands, and are now nitreous and intensely hard ad splitting like glass. Similar are the quartzites deep in the upper Cambrian. The Vermont red quartzites are red in color

and my mind is charcter like the Triassic of Conn, but are not cryptomeric. Then too these are more equally folded and are but little con- folded. The parting layers are thin red shale jmes that are usually sun-cracked. Some ripping of an undistinct nature is seen. Juber. Hummer is our geoin point. This was at Jonesville and Charlotte. Can this red quartzite be the eastern shore those of the Potsdam? See if any other fossils occur other than Phycosporia adanasi. At least 300 feet in known, , but as nothing has been seen nor what the formation sets upon, the total thickness is not known. To morrows we are to go to Ironton, Pailus Quarry, and Highgate Falls. May be Daniel got more help here. The L.C. dolomites seen this after noon are all crystalline, from fine grained to coarse, some are away white, and others are colored dark with darker Hatches. In one place we saw much truculent black chalk disposed in the dolomite quite irregularly as if a cryptogamate! It must be a diagnostic sign. Staying at Stiles Hotel at Milton, IT.

August 9-1921. Tuesday. A fine bright morning, and at 6.30 we are off for the north. Did all from mouth in the first 7 miles north and southbank of Milton. Saw a great deal of the Lower Cambrian dolomites, sandy dolomites and intraformational conglomerates. The dolomites are always thick bedded and usually dark hue color. The sandy dolomites are lighter gray and more thinly bedded than the pure dolomites. The peculiar feature of these is their sand which is coarsely granular in size and always more or less rounded. The dolomite conglomerates are very variable in the quantity of the pebbles. Frequently they are angular irregular pieces of two to three kinds of limestone and dolomite, and at other times the pieces are thin, flat and like those of the Bellman town intraformational conglomerates. These flat pieces more often lie flat, but may be at all angles, and sometimes cut into bedding. They then take on the character

I advise employees, the pieces are of all sizes from very small ones to three 3 to 4 and even 6 inches across. Sometimes these cylinders are badly squeezed and drawn out. They are the ochrestone where the pellets are much thinner and more elongated. See my sample. These flat pellet conglomerate have the pellets usually of limestone, and one wonders when the limestone were came from some such formations are not to be seen. Are they probably the semi-crumbled limestone of a year or two of accumulation not far diaforetically attuned to dolomite before entire cement in the dolomite? Extra get thought me for aug li at Shipgate Forky. The gravel conglomerate seen not far from Senjia Center are most interesting because of the quantity of pellets, their large size, and the little dolomitic parts that find them together. Some of the blocks are 8 feet long and the others divisions may be 6 and 4 feet. They consist of three kinds of dolomites, of the older formations. However one sees no flumar sand rock, nor brown white quartzite, and nor

whole pebbles, the granite rocks, All is either definite or of the quartzites interbedded with the old limits. Evidently no other rocks were exposed. The pebbles tend to be angular but the large blocks are somewhat rounded. At first one thought ice was the agent of transportation, but I will now concluded as below these conglomerates are local that torrential rivers was the form of transportation. In a local limestone conglomerate - the first one seen truly - I formed rock for more than two hours to get fossils. Reith for the first papers and after all my work I got 2 or 3 specimens of Ptychaspis or Glenflema birkens or may just spins, a large tail like Olenoides and Smithy, the tail of Bathynotus, Dancy where have seen Tridillatrogensis. On this conglomerate follows the great third area of L. Oldslates. It is in the lower 100 foot of the slate that these fossiliferous conglomerates occur,

It is our custom that the L.C. slate follow directly the dolomite series. The succession is thus: Permian and quartzite, Brinrock Marble, the first dolomite [illegible], the local conglomerate, and then the thick slate series (3000 ±). This makes at least 5600 feet of Lower Cambrian are Upper Cambrian. Stopping one night at St. Altaus, at the American House. [In 1923 Keith published a paper] saying that the St Altaus conglomerate me = Parotgian and hence all of the Beqjin slates are Parotgian. Therefore if the above only 2600 feet in Lower Cambrian and the 3700 feet of Beqjin slate an earlier Ordovician = Ogardian of Keith. [The field work of 1922 showed that the Milton dol. is Upper Cambrian, and that the Brinton Cong. is local Ordovician. The Ogardian lies below the Lowerm conglomerate.]

August 10-1921, Wednesday. Started north for Highgate Falls, the distance is 8 miles. For nearly 6 of it are over the Blue Limestone conglomerate, the "Giant Conglo- merate". At six miles north we came upon a little [illegible] (Rocky) spot, little [illegible], to the west of the road, exposed marble. It was undulating by tumbled slabs and contain by the Blue Limestone conglomerate. This marble replaced a length of 120 feet by 30 to 40 feet^[ and the thickness must have been 10 feet or so. The question at once arose is it a boulder or is it a piece of the old ground over which the Blue Limestone conglomerate is laid. It seems to type to be a boulder of any Alpine type of placers. Finally Keith was disposed to regard it as a piece of the old floor of the second cycle of sediment (= Mo. Cambrian to Trenton) let down to the east during Triassic faulting. [Later we also came up with this idea] I relay on again saw many fire exposures of the Giant or Blue Limestone conglomerate. As a rule the pieces are far than Blue Limestone, and

"The pieces are laid down at all angles, often the stand edgewise. Some of these pieces bear Lower Cambrian fossils, and in one block I got Ptychomenus and Lingulella. The most abundant pieces are of a white tridoye like limestone, the same as the great block seen 6 miles north of St. Albans. Finally there are pieces of the sandy dolomite and of a black colored dolomite, one much further down in the Lower Cambrian series. Again are some on or schist, no granite. Some of the boulders of the marble like li. are five to six feet long. We also saw some blue black shale pieces included in the conglomerate. The great majority of pieces are angular. Beneath the blue li congl. we often saw a rounded dark slate, that in places seems interlaid with gritty sand in the beds. For these various occurrences ite appears there is but one explanation. It is of true mile recurrence to be of cliff origin, at the same offer true of torrential rivers. At 6 1/2 to 7 miles north of St. Albans we saw much black slate that was gray similar to the others, but it has nothing whatever!

"Cambria"] To Dr Smith, it. [Next year it turned out to be Dufferin] At Highgate Falls there is a fine exposure of almost all the strata seen during the first three days. The Blue Lias conglomerate is well shown here in section towards the overhanging cliffs, of the river side, at least 100 feet down are pin & twig beds. Shales come in a thick series of black shales, with an occasional thin dolomite band. At the bridge is another conglomerate, but much higher than the Blue Lias conglomerate farther down stream. Towards evening saw for the first time an exposure of the brinrock marble about 100 feet in exposed beside the trolley line between Downton and St. Albans. Above it comes in a very long folded dolomite that weather admirably. See Keil's interpretations, mounted as a loose sheet here. Probably the entire thickness seen at Highgate Falls exceeds and 1000 feet. The best explanation of these conglomerates.

is that they are of glacial origin. This is the more certain of the "Giant Conglomerate" than of the salmon island older dolomite conglomerate. On the other hand there are some intraformational conglomerates. All in all the evidence is not yet fully in hand to explain the origin of the two main conglomerate groups. The banded nature of the sandy shales beneath the Giant Conglomerate are also evi- dence of glacial origin. Occasionally one sees a large boulder in these shales. Pieces of this shale and up to 3 feet long occur in the giant conglomerate. This conglomerate has a variable thickness, and in one place [where the large mass of marble occurs] at least a thickness of 40 feet is seen.

American House IRVING J. WRY, PROPRIETOR THE AMERICAN HOUSE AND ANNEX HAVE BEEN REFURNISHED, BATHS ELECTRIC LIGHTS AND SAMPLE ROOMS. St. Albans, Vt. August 10 1921 Swanton & [illegible] Blue Li. Conglomerate [illegible] SS, and thin Li. and Ord. r.s.s = Normal Dol. l.c.g. Georgia St. Burlington & Lower Cambrian Upper Cambrian - Ordovician. Interbedded dolomite and marbles. Windsor ma r.s.s Fault / Trace Snake Mt. Middleb Taconic folding H.Lawrence thrust fault, n.g. r.s.s ```</thinking> ```json {

August 11-1921. Thursday. Left St. Albans at 10.15 for the Parkers farm quarry, then the Hurland farm, and now the Montcalm farm. The latter purchased the place last year and are French Canadians from east of Ottawa. This farm is in the north- north-western corner of the Milton Quadrangle, 2 miles north 60 degrees west of Seneca Centre. The largest slate quarry is back in the field near a large elm tree in hard blue slates. Another one is half way up the hillside near the road and two other small slate quarries are beside the road. In the latter we got three backspuds (see list of faces end of this book). in the others we saw nothing. The slate bed has a considerable thickness, probably so far can be seen but apparently there is much more. Above the slate come micaceous, thin-bedded dolomite beneath the ^ that are more crumpled than any of the other rocks. In these occur may iron rock nodules = pure dolomite

modules, and one of the topmost i fsses an abs sim rust, &for four things (see list at end). Copying all these beds is a solid bed of salmon colored fine grained dolomite, about to fur thick. These shales have here a wide distribution and are but little crumpled or metamorphosed. Fossils of value can be had only after a long search and protracted quarrying. Of the Lutoginia bed saw nothing. We then machined further south and went along a little used and once a low private road. Along this road about 2 3/4 miles broad or degrees west of Senjia Center we saw pland upstreams of Minorotti crushed dolomite, see the samples. Here are occasional near white beds 2-4 fur thick interbedded with the typical Minorotti. Driving along the road to its end on the crest of the higher land facing the low land of Lake Champlain, and then going down the hill (then 3 miles west of Senjia Center) one can see a fine contact of the Minorotti

dolomite on the blue slate mount [illegible] dolomite. Dome not knowing the patrol would come sus- p[unclear]ect here between dolomites that this bedding like plane in the fault surface of the foot St. Lawrence = Logan or thrust fault. The plane of this thrust is here hardly more than 20 degrees. Further more there is no further deformation of either dolomite, nor did I notice any [illegible] crossing. The Brindwell dolomite in [unclear] at least 150 [illegible] feet thick and then maybe 200 feet of it. No Mount Real quartzite is present. He then drove rapidly out to the main road and thence 8 miles to Orwell, and 17 more to Burlington, and thence 6 miles more east to Essex Junction. Put up at a good country hotel the Lincoln Inn. It rained much during the night.

August 12-1921. Friday. It is raining a little this morning and we proceed out to our car until after dinner. At 1.30 P.M. we are off for Montpellier. At the falls of Brinashi river in Essex Junction there exposed much dark and light grey diorite. Ore unknown. An ore thurst is said to occur here, but a search for it failed to reveal it. Less than 2 miles east of Essex Junction appears a pegmatite -- a fist and fine emporment made up of quartz, feldspar, and some cord - thus is originally metamorphic. The alteration is least to the south and increases to the east. It is seen in for many miles, and even from some miles to the south out -- to about 2 [illegible] miles east of Bratbury. Towards the east it becomes much transformed into a schist. Then appear sericitic phyllite with zones of Haal phyllite. About 2 miles east of Bratbury occurs black phyllite of which I have a sample. All of these rocks are of Portuguese age. The Haal phyllite may belong to Ord. age.

At Northfield and for several miles to the South is a slate belt, quarried, and at about one mile south of Northfield we visited a small quarry. Have three samples. Here the schist- Troite is that of the bedding. This is the region in which Prof. Richardson got propylite. Since this black phyllite is of Ordovician age much of the sericitic phyllites only also are of the same age. We saw east of the Green Guts or quartzites, not dolomites, only a great thickness of phyllites. Since these Black Phyllites are of Ordovician age it is probable that the same kind of rock to the west of the lower Gut is of the same age. From Northfield south to Randolph we constantly see the sericitic and black phyllites. This for the reason that the road runs along the strike of the rocks. We are stopping at Randolph at the Randolph Inn. The widely extended pegmatite schist of

Post-auric age originally seems to have been in part an arid sea, and largely a dirty quartz sand. Such materials with the presence of feldspar leads to the conclusion that they are of post- murian deposition. This maybe so, but it should not be forgotten that then there was no land ardence to decompose the field spars. Thus the these deposits may afterwards be a delta or been a shallow sea deposit. It may well be that all of the Cambrian and Ordovician rocks of the Appalachia syn- syncline change towards the east to mud- stones. This will explain the absence in the Green Hills of limestones and dolomites, and the great thickness of sandstones here.

August 13 - 1921. Saturday Left Randolph at 9 A.M. and passed through Bethel, Royalton, Sharon, Deer Hill Pond, Hartford to White River Junction. Here at 1.00 P.M. took the train to Springfield, Mass., where changed cars for Deer Haven. Left here at 7.30 P.M. Two miles southeast of Randolph are entered a belt of highly metamorphosed shales with interbedded limestones. In these further north Richardson has found Ordovician fossils. Further east are the sericitic and hornblende schists described by him before. One-half mile south of Royalton are entered the belt of Patersonic gneisses metamorphosed to garnetiferous stromatic schists. Granite renews at Sharon, and at about one mile east appear phyllites of the Patersonian. Further north the renews are the way to the Connecticut River.

August 11-1921 Parkers Farm in Micaceous then reddish dolomite. Arisus ia festinata (Billings) 1 sp. Styloites americanus (Billings) 1 sp. Bathynotus holopyga (Wall) 3 tails Agraulis strenua Billings 1 head August 11-1921 Parkers Farm in slate along trail Ohtella crana (Wall) 1 sp. Acrotrita sajjttolis taconica 1 sp. Was in Vermont again late in July 1922. See another book.

No text detected

New England Intercollegiate Trip. October 14, 1921 At one P.M. started out in Deutars car with the Knoffs for Attleboro, Mass.

No text detected

No text detected

No text detected

No text detected

Rufford Q. 2m nbs of Sevin Cat. Drinks 23/0 m. Dr. so Dr. J Segue Cate. 3m. more of Seve Cate.

No text detected

3038\frac{1}{2}

No text detected

No text detected