near the crossing of Blood's Brook next the argillite has the dip 75° N. 60° W. Cupreous schists are seen in several places in Norwich. Many small crystals of magnetite occur in sericite schists in the valley west of the railroad station, dipping 50° N. 70° W. At the tannery the strata are vertical with the strike N. 60° E., being quartzites and chlorite schists. Near the gristmill the rock is chloritic and dolomitic, 65° N. 60° W.

Section 2 shows an actual contact at the river between the hornblende and sericite schists, 60° N. W., followed by sandy and chloritic schists and the following positions in order, 70° N. 57° W., 90° dip N. 30° E., 50° N. 20° W., 80° N. 70° W. There are three folds apparent in these rocks, in a section from the heights back of Hartford village to Craft's hill in Lebanon. Many of these rocks are diorites and diabases, and for awhile we tried to convince ourselves from a study of the microscopic sections that these were remains of protozoans analagous to Eözoon. Later investigations made it clear that these rocks were of truly igneous origin, such as would render the conditions unfavorable to the preservation of organisms and hence our fossils went to keep company with the Eözoon of the Laurentian, now universally admitted to be purely a mineral development.

The deeply incised valley of the White River has cut through great vertical thickness of these green rocks and made them accessible to investigation and are best seen on the north side of the river. The most easterly exposure is a coarse, chloritic rock on the west border of the modified drift, projecting itself through the sand west of the top of the long hill north of the Junction village and west of the camp-meeting ground.

The divisional planes belonging to these rocks were not made out. Near the cemetery on the road to Hartford are chloritic schists dipping 76° S. 40° N. Next east of E. C. Watson's are feldspathic rocks, chloritic quartzite, epidotic quartzite, chloritic schist, argillitic and sericite schists. There is a quarry at the roadside close at hand, represented in Plate XXIII, where the strata are vertical with the strike, N. 35° E. The materials are hard green quartzites, some parts of which exhibit folia of epidote, light gray sandstones, chloritic schist, sericitic quartzite and sandstone. There are jointed seams dipping northerly directly across the strike of the stratification. They are spoken of because they are sometimes imagined to be strata and everyone interested can see the relation of the two sorts of planes in the plate. At the iron bridge are strikes N. 30° E. and N. 60° E.

The best dip is 65° S. 60° E. The schists are cut by dikes of diorite, are much broken by faulting, but the blocks are cemented together firmly. This state of things may represent the conditions prevailing all over the region; the rocks have been fractured everywhere, but the blocks have been cemented together so closely that they will not separate any more readily along the planes of fracture than elsewhere. The individual blocks may vary in size from a brick to a township. The country has, therefore, been subjected to repeated and violent earthquakes in its early history. The ledges under the iron bridge represent the west border of the chloritic schists; the argillites come in just below the dam. South of the river at the Hartford station of the Central Vermont Railroad are fine illustrations of bent strata, exhibited in Plate XXIV. Similar ledges appear along the Woodstock Railroad a few feet higher up. These rocks may represent the

transition from the schist to the argillite.

The relations of this formation along White River, as just described, are shown graphically in Section 3, Plate XXIVa.

Nearly two miles southward from the Junction are two conical summits, each 700 feet high. The east one is composed mainly of hornstone and a compact diabase which suggests an igneous mass such as might be called the base of an ancient volcano. The western one is probably identical in character with this. And there are two similar cones in the very southeast corner of Hartford, of which the more eastern is a protogene carrying inclusions of green schist, so indestructible as to make a great bend in the river. There must have been another scene of igneous activity at the falls of the Quechee near the woolen mill at North Hartland, where green schists running nearly east and west have been cut at right angles both by the more compact diabase and dikes allied to camptonite.

A section across the chloritic group near Kilburn brook about two miles from the Junction gives us hornstones close to the Connecticut River, dipping 80° N. 80° W., 70° N. 60 W., at the brook itself chiefly hornblendite, 75° N. 80° E., less than a mile back from the river, and vertical schists on the Hartford-North Hartland road, at the east base of Neals Hill. This gives a synclinal altitude to these schists along the line of Section 4, Plate XXIVa. This formation crosses the Connecticut at North Hartland. In the river are remnants of green schist resembling the piers of a bridge, dipping westerly, and northeast at the "Hen and Chickens." The rock may be traced southerly into Willard's ledge and Prospect Hill in Plainfield. It is a compact diabase at the ferry, a green diabasic schist on the