basin of Raritan is included, embracing more than two-thirds of that state, is a slope of 140 miles from south to north, mean width about 25, and area 3500 square miles.

Of this slope, from Cape May to Sandy Hook, the Atlantic shore, with a slight elliptic curve outwards, preserves a similar character with the coast of Maryland, Virginia, and the Carolinas. Long, narrow sand islands stretching in a chain outside of shallow and narrow sounds. The inlets, numerous between the outlets of the Delaware and Hudson, are, however, shallow, admitting only a coasting navigation. The tides, sweeping round this almost insulated tract, penetrate the smaller rivers only 15 or 20 miles. The remark may be repeated, that the peninsulas between Chesapeake Bay and Delaware Bay, and that again between Delaware Bay and river, the Atlantic Ocean and Hudson Bay, differ from Long Island only in the circumstance of the latter being separated from the continent by a sound. Suppose the others cut off in a similar manner, and the resemblance will be obvious to the most casual observer.

The very remarkable basin of the Hudson follows that of Delaware and the Atlantic slope of New Jersey. Forming the great link between the Atlantic Ocean and the vast basin of Canada, the Hudson basin has that of Delaware south-west; the extreme north-eastern part of that of Susquehannah on the west; that of St. Lawrence north-west, north, and north-east; the basin of Connecticut east; that of the Housatonick south-east; and the Atlantic Ocean south. In Lat. it extends from the south ern end of Staten Island, 40° 30', to the extreme fountains of the main Hudson, 44° 8' North. These two extremes, lying very nearly in Lon. 3° East from W.C., stretch also along the greatest length of the basin, or to an unimportant fraction of 250 miles; mean width 55, and area 13,750 square miles.

The physical features of this basin are in a very striking manner curious. Like that of the Delaware, the Hudson Basin extends very nearly from south to north; but the Delaware basin rises from the primitive ledge by gradual acclivity, whilst the tide valley of the Hudson is protruded inland over the primitive to the margin of the central secondary. Some of the peculiar features of the Hudson basin were noticed under the general view of the Appalachian system, and by reference to what was observed under that head, it will be seen that the deep tide vale or narrow bay of the Hudson is a part, about one half of an immense chasm in the continent of North America, extending from the Atlantic Ocean, in a direction a little east of north to the St. Lawrence. Along this chasm the tide is borne inland 160 miles to near the junction of the two main branches of the Hudson. Beyond the head of the tide, the valley or channel of Hudson Proper, rises gently for another stretch of 40 miles. Thence rises a neck of land, 18 miles wide, which intervenes between the basin of Hudson and Lake Champlain, but even here the summit level does not rise to 141 feet above the tides in Hudson river. From these observations it must be seen that the

Between the sources of Esopus creek and those of the Schoharie, or southern branch of the Mohawk, rises that remarkable mountain nucleus, particularly called the Catskill Mountains. This group, though of a less extent, is specifically similar to the valley of Mexico, and the European valley of Bohemia. Some of the peaks rise to near 4000 feet, and the main mass rises between 10 and 25 miles from the tides of the Hudson, 40 miles below their head.

From this comparatively very elevated tract the Schoharie is poured northwardly into the deep vale of the Mohawk. The latter, by its channel extending from the main stream near the head of tidewater, in a direction a little north of west, carries a chasm in the continent, rising in no place to 426 feet above mid-tide level in the Hudson. The Mohawk has interlocking sources with the Susquehannah Proper, Unadilla and Chenango, with the confluents of Oneida Lake, and those of Black river. The upper branches of the Mohawk flow towards each other and unite on a table land, where, whilst in a state of nature, the water in times of flood separated; part flowing to the westward into Oneida, and thence by the Oswego, or Onondago river, into Lake Ontario; whilst the other part flowed down the Mohawk into the Hudson.

This table land between the Mohawk and Oneida Lake, is the lowest depression in the Appalachian system, and at right angles to its chains, from the south-western termination of the system to the Saint Lawrence, near the confluence of that great stream and the Ottawas, and has been, to the honor and incalculable advantage of New York, made the route. of part of a canal uniting the Hudson tides to the water of Lake Erie. To this, the still deeper depression of the Hudson and Lake Champlain route is no exception, as the latter extends evidently along, and not at right angles to the mountain vallies.

The Hudson in full contrast with the Mohawk issues by numerous sources from the Sacondago chain, and from a rather elevated table land, cold, sterile and forbidding. The region from which flows the Sacondago and Hudson Proper, the sources of Oswegatche, Grass, Racket and St. Regis, into St. Lawrence, and the Sable and Sarenac rivers into Lake Champlain, is perhaps the least inviting tract in the United States. It abounds in mountain ridges, lakes and marshes, giving source to streams which find their respective recipients on borders of an entirely different character. This moist, cold, and repulsive region has remained in great part desolate and unsettled, whilst improve

ment has rapidly advanced around its outer circumference, or along the outlet of its rivers.

The entire western slope of the Hudson basin so diversified in feature, latitude and elevation, stretches 250 miles from south to north. Where widest along the valley of the Mohawk, it is 90 miles in breadth, but narrowing to the northward, and still more to the southward of the Mohawk valley, and the area being 9500 square miles, the mean breadth is 38 miles.

The eastern slope of the Hudson basin extends 170 miles from Haerlem river or strait, to the sources of Batten Kill, with a mean width of 25 miles; area 4250 square miles. Between Haerlem river and the Blue Ridge, or, as there called, the Fishkill Mountains, Croton river and some smaller creeks, drain the eastern slope of the Hudson. Above the mountain pass of the Highlands, this slope is limited to the eastward by the Blue Ridge, and is drained by Fishkill, Wappinger, Ancram and Kinderhook creeks; and thus far the Hudson basin is opposite to that of Housatonick: but north wards of the sources of the latter river, those of Hoosack and Batten Kill originate in the continuation of the South East Mountain, there called Hoosack Mountain; the same chain known still farther northwards as Green Mountains.

To an eye sufficiently elevated the whole Hudson basin would present a most interesting appearance. The main channel, in particular below the tides, generally a deep chasm lined with immense walls of rock. So deep indeed is this long narrow bay as to be very seldom visible from the roads along either shore. This chasm is not as on the St. Lawrence the lowest depression of a gradual declivity from the outer exterior border of the basin, but an abrupt fissure in the rocky base of the whole physical section. The rivers and creeks flow moderately until near their recipient, and are then precipitated with great rapidity, yielding two long series of water falls, and affording, perhaps, the most extended water power in the United States.

Into this profound chasm, ships of nearly the heaviest burthen can be navigated above the Highlands, and sloops to Troy, within 2 miles off the confluence of the Hudson and Mohawk, and from its surface so little can be seen of the enchanting prospects which abound over the basin on both sides, that the voyager feels, for hours, as if immured between craggy and precipitous walls of rock. At intervals, however, glimpses of the distant mountain, the cultivated fields, the neat and flourishing towns, the dashing water fall, and the elegant villas crowning the steeps; all give intimation of the rich and varied regions beyond the limits of vision from the river surface. But to resume our general survey.

Under the head of Appalachian system, it was shown that the physical sections on each side of the Hudson were united by the mountain chains, though a tide channel did in one place pass over a gap in the system. On some other points of view, that region of North America, bounded on the southwest by the Hudson, Lake Champlain and Richelieu river; on the north-west by Saint Lawrence

river; north-east by the Gulf of St. Lawrence, and east, south-east and south, by the Atlantic Ocean, has so many peculiar features as to constitute a very distinct physical section. This section approaches a parallelogram of 500 miles from south-west to north-east, and with a mean width of 200 miles; area 100,000 square miles. Politically it contains of the United States, the eastern slope of New York, with all Connecticut, Rhode Island, Massachusetts, Vermont, New Hampshire and Main; and of the British North American possessions, the south-eastern slope of Lower Canada, and all New Brunswick, and Nova Scotia. Exclusive of the peninsula of Nova Scotia, which is very nearly insulated, the main body of the natural section under review is divided by its rivers into two very unequal slopes or inclined plains. That which rapidly falls towards the Saint Lawrence, is a strip of 560 miles in length; the utmost breadth along the valley of Saint Francis river, about 100, but where narrowest, between the extreme northern sources of St. John's river and the channel of St. Lawrence opposite the mouth of Saguenay river, not quite 10 miles, and perhaps overrated at a mean width of 50, and area 28,000 square miles. The largest and longest river of this confined slope is the St. Francis, heading with the Connecticut, and having a valley of about 110 miles in length.

The opposing slope, with a declination very nearly southward, gives source and course to the great streams of Connecticut, Kennebec, Penobscot and St. John's, which have their remote sources in the dividing ridge between the Atlantic and St. Lawrence waters, and also to several of lesser length of course and magnitude of volume, that rise and flow in the intervals which separate the basins of the former and more considerable rivers.

The character of coast, prevalent from the outlets of the basins of Santee and Pedee to the mouth of the Hudson, is perpetuated along the north-eastern shore to Cape Cod inclusive; if we regard, as on every physical principle we ought, Long Island as the real Atlantic shore. Passing Cape Cod and entering the deep gulf between the south-eastern shores of Massachusetts and the south-western of Nova Scotia, a new order of coast commences. The ocean border, hitherto a sandy flat, or where rocky or more elevated, the elevations moderate, now becomes bold and prominent. The points and intervening bays numerous, and harbours deep and safe.

One of the most remarkable, and, whether regarded as a natural phenomenon or as influential on the operations of man, the most important, may be appropriately noticed in this place. The Atlantic tides from the Bahama channel, along the coast, increases in height, advancing north-eastward. The increase, it is probable, if not disturbed by the irregular protrusions of the land, would follow a nearly regular law of progression, and this is with some allowance the case between very prominent points. From the Bahama channel to Cape Hatteras, the increased height follows a scale but little influenced by the moderate intervening projections; but passing Hatteras the increase is at once very

rapidly augmented. The tides, however, again resume and follow a regular ratio of increased height, with slight deviations to Cape Cod.

From the Florida point, where mean tide does not exceed, if it amounts to two feet, to Buzzard Bay, on the south side of Cape Cod, the increased height has reached an extreme of 9 feet. Viewing the Gulf between Cape Cod and Nova Scotia, with its retiring bays and salient points, and without any knowledge of facts or their causes, we would be unprepared to expect the tides to be doubled in elevation, on passing the narrow neck between Buzzard and Cape Cod bays, yet such is the fact. The gulf, which to avoid circumlocution we may call the Gulf of Maine, extends from Boston harbour to the coast of Nova Scotia, 250 miles, and if extended to the head of the bay of Fundy, upwards of 400 miles; its depth inland about 140 miles.

Into this wide mouthed gulf the waves of the Atlantic Ocean pour with inconceivable elevation and force, and retreat again with corresponding violence. Rapidly as the mean height of the tides south-west from Cape Cod augment, advancing from south-west to north-east, their increase is still more rapid from the bottom of Cape Cod bay, to that of Fundy. The actual mean and extreme tides of Fundy have been, no doubt, exaggerated greatly, when their lowest term is given at from 30 to 40, and extreme from 50 to 60 feet; but retrenching one half, would leave this tide volume far the most elevated on earth.

What are the causes of the increase of the Atlantic tides along the coast of the United States and New Brunswick, and their great excess at the northeastern extreme?

These questions remain desiderata, and without pretending to determine such a problem, it may be suggested, that the Gulf Stream is the immediate cause. This oceanic current at its outlet from the Gulf of Mexico, between Florida and Cuba, is met, increased and turned along the Florida shores, by another current between Cuba and the Bahama islands. Confined to a width of from 40 to 60 miles, until clearing the whole Bahama chain, the Gulf Stream is rapid, and for the next 500 miles of its course, across the elliptic gulf in front of Florida, Georgia and the two Carolinas, though the stream widens and of course weakens, it still retains sufficient force to lessen the height and deflect the course of the tide.

Between Cape Hatteras and Cape Cod sweeps inward another elliptic gulf, of not much less length of chord than that between the Bahamas and Hatteras; along the second, or as we may call it, the middle Atlantic Gulf of the United States, the great ocean river flows with an expanded breadth and diminished elevation, and here the land swell is found to have increased in direct ratio with the diminution of the Gulf Stream.

Into the third, or Gulf of Maine, at the distance of 1000 miles from the northern outlet of the Bahama channel, the accumulated tides are left to fall with their whole weight, as opposite to its front of 250 miles, the force of the Gulf Stream has become almost negative.

Whilst, whether the preceding is in whole or in part a solution of the phenomena of the Atlantic tides along the coast of the United States, New Brunswick and Nova Scotia, remains for future investigation, we may notice a very remarkable and salutary effect of the increased height and, of course, violent ebb and flow of the tides on the coast of the Gulf of Maine. From the lower harbours of Chesapeake Bay, inclusive to the southwest, the navigation of the United States is not materially interrupted by ice, but from the Delaware inclusive to the north-eastward, the harbours and rivers are liable to be closed or greatly obstructed by winter frosts. Were it not prevented by the peculiar phenomena of the tides, the interruption from ice would augment with the latitude; but the very violent currents produced twice in every astronomical day, by the tides along the shores and in the tide part of the river channels and bays, prevent the formation of solid or compact fields of ice. This is evidently the cause why, that in severe winters, the harbours of Massachusetts, New Hampshire, Maine, and New Brunswick are more available for navigable purposes than are those of Delaware, Pennsylvania, New Jersey, New York, Connecticut, and Rhode Island, or those even of Massachusetts to the south of Cape Cod. With these remarks we return to our general survey.

Both in our review of the mountains, and of the Hudson basin, we have shown that the latter was separated from the physical section last noticed, by the continuation of the Blue Ridge and South East Mountain. If we extend our view beyond the estuary of the Hudson, the first remarkable object which meets our eye is Long Island. That the Chesapeake and Delaware peninsula, the Delaware and Hudson peninsula, the Massachusetts peninsula, and Nova Scotia are all specifically similar to Long Island, has already been remarked. Though on a much more contracted scale, similar resemblances exist in Staten Island and Manhattan island, the latter rendered of so much importance from having on its surface the city of New York.

Long Island lies between N. Lat. 40° 34′ and 41° 10', and Len. 2° 58′ and 5° 08′ E. from W.C. The mean range is N. 694° E.; utmost length from the Narrows to Montauk Point, within a trifle of 120 statute miles. The utmost width nearly along the line between Queens and Suffolk counties, 20 miles; the mean width about 8, area 160 square miles.

The deep sound which separates Long Island from the continent, bears a strong resemblance in extent and form to the island, and both are followed by a bold and rather abrupt coast, the outer abutment of a slope, down which flow Housatonic, Connecticut, Thames, and the smaller rivers entering Narraganset and Buzzard Bays.

Housatonick comes first in order, advancing eastward from the Hudson. The mountain chains now stretching from south to north, discharge the rivers southwardly along their intervening vallies. The Housatonick, interlocking sources with those of the Hoosack, on the table land of Berkshire, at an elevation of from 900 to 1200 feet, and between the South East Mountain and Blue Ridge. From this

elevated source the Housatonick flows, by compative courses, 65 miles, in a direction a little west of south, and in a striking manner parallel to the Hudson and Connecticut rivers; thence piercing the South East Mountain, the Housatonick bends to a course south south-east 40 miles, to its efflux into Long Island Sound, after an entire comparative course of 105 miles.

Wallingford basin, from the brevity of its confluents, would not deserve specific notice in a general view, were it not rendered important from the fine city of New Haven, and from a proposed communication by canal between its principal tributary, the Quinipiack, and Farmington river and canal. The Wallingford basin, only 30 miles in length, intervenes between that of Housatonick and Connecticut. Confined, however, as it is, the basin of Wallingford, at the distance of ten miles, is separated from that of Housatonick by a chain of mountains, and again it is detached from that of Connecticut by another chain still more elevated and distinct; both chains exemplifying a remark formerly made in this article, that the Appalachian chains, eastward of the Hudson, extended nearly at right angles to the Atlantic coast.

Taken together, the two basins of Housatonick and Wallingford may be truly considered a mountain region, extending in Lat. from 41° 08 to 42° 34' N., and in relative elevation differing 1200 feet. Such, indeed, is the abrupt rise of the plain from the Sound, that the tides rise but a few miles in either basin.

Both the preceding and the Hudson and Champlain basins are followed by the long and interesting basin of Connecticnt. As laid down on Tanner's United States, the Connecticut has its highest source at N. Lat. 45° 15', and enters the Sound at N. Lat. 41° 16'; of course flowing over within an insignificant fraction of four degrees of latitude. The basin lies between 4° and 5° 45′ E. from W.C.

So little does this stream incline westward of south, that in its entire length, or rather direct line from source to mouth, of, by actual calculation, 277 statute miles, the course is S. 12° 18' W; nor does the stream in any part of its course depart 40 miles from a line drawn direct from source to outlet. The comparative length of the channel, determined by steps of 50 miles, is almost exactly 300 miles. The length of the basin is 290 miles; and in one part from the sources of Chickapee river to those of Westfield river, it is 60 miles wide, but narrowing gradually towards both extremes, the mean breadth is perhaps not far from correctly estimated at 40 miles; area, from the preceding elements, 11,600 square miles.

This beautiful stream has interlocking sources with those of St. Francis and Androscoggin or western branch of Kennebec river. From this elevated source the main stream flows by comparative courses, 70 miles to the influx of the Passampsic at Barnet Falls. The real elevation has never been well determined of the region from which are derived the sources of Connecticut, St. Francis and Androscoggin, but the height of the former at Barnet Falls has been found by actual measurement 420 feet above tide water at Hartford. At pages

13 and 14 of Armroyd's Internal Navigation, the following elements are inserted. In a direct distance above Barnet or M'Indoe Falls, the rise is 386 feet; thence in a distance of about 50 miles, following the channel from Dalton to Stewardstown, the rise is 222 feet, and from thence to Connecticut lake, above 30 miles along the channel, 562 feet. The entire fall from Connecticut lake to Barnet 1170, which, added to 420 below Barnet, gives an entire fall of 1590 feet from the level of Connecticut lake to tide water. The lake is not, however, the utmost extreme or clevation of the basin, which, it is probable, reaches, if it does not exceed, 2000 feet. The difference or level is fully equivalent to four degrees. of latitude, giving to this basin as respects aerial temperature the extremes of eight degrees of latitude, or considerably more than exists in any other river basin of the Atlantic slope of the United States.

As far as the defective delineation of the mountain chains on our maps will enable us to trace the connexion, it appears that the chain which leaves the Sound between the basins of Connecticut and Thames is continued northwardly, separating in its advance beyond the Thames, the basin of Merrimac from that of Connecticut, but traversed by the latter stream between the falls at the mouth of Passumpsic and Lancaster, and thence more northwardly, separating the vallies of upper Connecticut and Passumpsic. The preceding conjecture is strongly supported by the relative elevations of the latter stream and the surface of Lake Memphramagog, with their intervening summit level.

Passumpsic river rises on a table land interlocking sources with those of Willoughby river and lake, one of the higher confluents of Lake Memphramagog, and flows thence southwardly 25 miles, to its junction with the main Connecticut. The summit level between Willoughby Lake and the source of Passumpsic is, according to Armroyd, 523 feet above Lake Memphramagog, and 755 feet above the water at the confluence of Passumpsic and Connecticut. If these elements are correct, the summit height which separates the valley of the Passumpsic from that of St. Francis, is 415 feet below Connecticut lake, and from all analogy double that descent below the extreme fountains of Connecticut river. They also expose another interesting feature in the surface of this region; that is, that Lake Memphramagog is 938 feet below Connecticut Lake.

From the preceding data, it appears that Connecticut river rises on a comparatively very elevated table land, and, passing a chain of mountains, falls upwards of 1200 feet in 60 direct miles, or upwards of 20 feet per mile, and that more than 200 miles above the head of its tides, the stream has made more than two-thirds of its entire descent. We have been more particular in our attempts to determine the real elevation of the region giving source to Connecticut, as the same elements decide the height, from which flow the St. Francis and Chaudiere into St. Lawrence, as also that giving source to the western confluents of the Androscoggin and Kennebec rivers, and more north-eastwardly to the higher sources of St. Johns river.

This tract is, in fact, independent of mountain ridges or chains, a real table land rising to from 1800 to perhaps 2200 feet above the tide level in the Atlantic Ocean. That part from which issue the extreme fountains of Connecticut lies very nearly at equal distance, one hundred and ten miles, from the head of the tides in the Kennebec, and that in St. Lawrence at the town of Three Rivers.

The great height of their fountains, compared with the brief mean length of their courses, explains the cause of the unnavigable channels of upper Connecticut, Androscoggin, Kennebec, St. Johns, Chaudiere and St. Francis.

Connecticut, however, pouring its rapid current down 1170 feet in the first 60 comparative miles of its course, has fallen at the mouth of Passumpsic, to 420 feet above tide water, 81 feet lower than James river at Lynchburg, 153 feet lower than the Potomac at Cumberland, 303 feet lower than the Susquehannah at Tioga Point, 35 feet lower than the Delaware at the mouth of Nevisink river, or where united with the Hudson and Delaware canal, and almost exactly, or at least differing only 5 feet from, the summit level of the Hudson and Erie Canal, on the Utica and Rome level.

If we compare these comparative elements with the length of their respective channels above tide water, and extend our view to the Alatamaha on one side, and to the Penobscot on the other, we shall find that, excepting the Hudson, the channel of the Connecticut, even in its natural state, is the deepest and most favourable navigable route on the Atlantic coast of the United States. It is, by the bends of the river, 220 miles from the mouth of Passumpsic to Hartford, and that distance has already been made navigable; but farther improvements are contemplated.

In proportion to its length, the basin of Connecticut is narrow, and the confluents from either side are numerous, but of no considerable length or volume. Advancing upwards along the western side, the first tributary of note is Farmington river, from Hartford county, Connecticut. Westfield river heads in the Green Mountains, opposite to the Housatonick, and falls into the Connecticut at Springfield; Deerfield river mouths below Greenfield: both the latter streams are in Massachusetts. In Vermont, the Green Mountains give source to numerous fine streams flowing south-eastwardly into Connecticut river, but none of magnitude above that of a large creek. The principal ones are West, Black, and White rivers. On the eastern side there is no stream worthy notice entering Connecticut river in the state of Connecticut. From Massachusetts enter Chickapee and Miller's rivers. From New Hampshire, also, the confluents are unimportant, if we may except the Asbuelot, entering the main stream at Hinsdale, in the south-western angle of the state; and the Amonoosuck, heading with the Merrimack and Saco, in the Green Mountains, and joining its recipient ten miles below the influx of Passumpsic. Thames, Narragansett, and Buzzard basins follow that of Connecticut along the same slope; but, if taken together, drain only a surface of 4250 square miles, of which the Thames basin occupies VOL. XVIII.-PART I.

1600, Narragansett 2000, and Buzzard 650 square miles.

The tide, which penetrates the Connecticut upwards of forty miles, is arrested in the basin of the Thames, at about 16 miles from the sound. Into the Narragansett, the flood of the ocean ascends to Providence, 30 miles, and about half that distance in Buzzard Bay.

Passing Buzzard and Narragansett, we find the singular projecting curve of Cape Cod, extending 38 miles eastward into the Atlantic, and thence 32 northwards, enclosing a deep bay bearing the same name. This bay is, however, only part of one of those gulfs or lengthened bays which indent the Atlantic coast of the United States, extending about 65 miles from the narrow neck of Barnstable, and from a line drawn from the extreme northern point of Cape Cod to Cape Ann, 25 miles in depth. Following the general bearings of the coast, the curve of this sheet of water is 150 miles, and, including the extension of Cape Cod, is bordered by a slope in no part 20 miles wide, and does not exceed eight miles of average breadth. The great and abrupt increase of the tides passing from the southward into Cape Cod Bay has been noticed; yet so bold are the shores, and great the angle of acclivity of the country, that the tide in no one place penetrates ten direct miles inland. The water inside the cape is generally shallow, but that from Plymouth to Gloucester inclusive, abounds in fine harbours, of which Plymouth, Boston, and Salem may be considered the principal.

With Cape Ann the slope greatly widens, curves first westward, thence a few miles to the northward, and finally to N.N.E.; and in a distance of 50 miles the coast is broken by the outlets of Merrimack, Piscataqua, and Saco: the two former, rising in the White Mountains, interlocking sources with each other, and with those of the Amonoosuck and Androscoggin rivers, and overheading the numerous confluents of the Piscataqua.

The White Mountains of New Hampshire have attracted attention since the original settlement of the country, and the extreme height probably accurately determined at 7300 feet above the Atlantic level; but the most important part of their physical history remains obscure. Are the peaks called "White Mountains" a detached group? or are they not like the peaks of Otter and Catskill mountains, part of an extended chain? The latter has in its support the analogy of other sections of the Appalachian system, and the great elevation of the country northwardly from the main group, and which separate the sources of Connecticut from those of the Androscoggin; and again, those of Kennebec and Penobscot from those of Chaudiere.

Leaving the preceding hypothesis to future investigation, we find the sources of two rivers pouring from the southern side of the main group of White Mountains. These sources are the higher fountains of Merrimack and Saco.

The Merrimack, Saco, and Amonoosuck rivers issue from within two or three miles of each other, at North Lat. 44° 10', and at a probable elevation of 4000 feet, on the slopes of the White Mountains.

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