EPA-R3-73-028C
MARCH 1973 Ecological Research Series
ANNOTATED BIBLIOGRAPHY OF
LAKE ONTARIO LIMNOLOGICAL
AND RELATED STUDIES
Vol. Ill Physical
LU
Office of Research and Monitoring
U.S. Environmental Protection Agency
Washington, D.C. 20460
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VftV
RESEARCH REPORTING SERIES
Research reports of the Office of Research and
Monitoring, Environmental Protection Agency, have
been grouped into five series. These five broad
categories were established to facilitate further
development and application of environmental
technology. Elimination of traditional grouping
was consciously planned to foster technology
transfer and a maximum interface in related
fields. The five series are:
1. Environmental Health Effects Research
2. Environmental Protection Technology
3. Ecological Research
4. Environmental Monitoring
5. Socioeconomic Environmental Studies
This report has been assigned to the ECOLOGICAL
RESEARCH series. This series describes research
on the effects of pollution on humans, plant and
animal species, and materials. Problems are
assessed for their long- and short-term
influences. Investigations include formation,
transport, and pathway studies to determine the
fate of pollutants and their effects. This work
provides the technical basis for setting standards
to minimize undesirable changes in living
organisms in the aquatic, terrestrial and
atmospheric environments.
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EPA-R3-73-028C
March 1973
ANNOTATED BIBLIOGRAPHY OF LAKE
ONTARIO LIMNOLOGICAL AND RELATED STUDIES
Vol. Ill - PHYSICAL
By
John Baldwin
Robert A. Sweeney
Project 16120 HVR
Project Officer
Norbert A. Jaworski
U.S. Environmental Protection Agency
National Environmental Research Center
Corvallis, Oregon 97330
Prepared for
OFFICE OF RESEARCH AND MONITORING
U.S. ENVIRONMENTAL PROTECTION AGENCY
WASHINGTON, D.C. 20460
For sale by the Superintendent of Documents, U.S. Government Printing Office, Washington, D.C. 20402
Price $2.60 domestic postpaid or $2.25 GPO Bookstore
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EPA Review Notice
This report has been reviewed by the Environmental Protec-
tion Agency and approved for publication. Approval does not
signify that the contents necessarily reflect the views and
policies of the Environmental Protection Agency, nor does
mention of trade names or commercial production constitute
endorsement or recommentation for use.
ii.
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TABLE OP CONTENTS
Page
I. Introduction 1
II. Subject Index 2
A. Study regions 2
B. Techniques 4
C. Instrumentation 7
D. Parameters 10
III. Abstracts 18
IV. Author/Agency Addresses 184
V. Other Possibly Pertinent References . 195
VI. Achnowledgements 207
LIST OP FIGURES
JL Page
1 Map of Lake Ontario 2a
iii.
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I, INTRODUCTION
The purpose of this study, which was sponsored under
grant # 16120 HVR from the U. S. Environmental Protection
Agency, was to provide a reference that would be of aid to
those individuals and/or agencies, planning or initiating
limnological research on Lake Ontario and/or its tributaries,
particularly those activities which are part of the Inter-
national Field Year on the Great Lakes (1972-7*0. The task
was divided on the basis of disciplines into three (3)
sections - chemical, biological and physical. This paper
is the final report from the latter.
The holdings of libraries in both the United States and
Canada xvere surveyed. Each pertinent reference was abstracteo.
and examined with respect to the parameters measured, tech-
niques employed and the location(s) in which the study was
conducted. In addition, the last known address of the agency
or senior author was noted for inclusion of locating the
author if further communication is desired.
Unless otherwj.se noted, the papers cited in the annotated
bibliography are located in Buffalo.
Due to limitations in time, we were unable to secure
copies of a few references that may contain information
relative to Lake Ontario. These have been included in this
paper.
-1-
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Comments concerning this work are welcome and
appreciated.
SUBJECT INDEX
The number following each, refers to the number of the
paper listed in Section II. Lake Ontario was divided into
eighteen (18) regions, which are shown In Figure 1. The
number nineteen (19) refers to lake-wide studies; while
twenty (20) concerns tributaries to the lake. For the
identification of the specific stream or river in question.,
see the abstract.
A. Study Regions
1. 16, 107, 1^5, 152, 165, 188, 195, 244. 246,
253, 260, 261, 286, 292, 316, 322, 338, 373
2.
13, 49, 56, 57, 59, 60, 94, 100, 107, 145,
152, 165, 188, 195, 198, 228, 244, 246, 252,
259, 260, 261, 262, 286, 292, 316, 338, 339,
3. 16, 30, 33, 51, 56, 57, 59, 94, 103, 109,
134, 145, 152, 165, 174, 175, 188, 195, 198,
200, 211, 229, 234, 238, 242, 246, 253, 26l,
265, 275, 286, 290, ?93, 316, 338, 339, 351,
372, 373, 387, 429, 438
4. 14, 49. 51, 54, 56, 57, 59, 131, 145, 161.
165, 188, 195, 198, 204, 217, 229, 244, 246,
261, 274, 231, 287, 316, 338, 339, 354, 373,
387, 430
5. 38, 51, 56, 57, 59, 142, 188, 246, 276, 316,
340, 358, 387, 429
6. 51, 54, 56, 57, 59, 60, 126, 188, 281, 316,
373, 387, 429
7. 38, 51, 56, 57, 59, 188, 246, 316, 340, 358,
387
—2—
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8. 51, 54, 56, 57, 59, 60, 188, 229, 316, 373,
387
9. 51, 56. 57, 59, 188, 233, 234, 264, 316,
331, 340, 358, 387
10. 33, 47, 51, 54, 56, 57, 59, 60, 103, 114,
115, 125, 127, 188, 201, 229, 283, 303, 316,
331, 338, 369, 373, 374, 375, 387, 436, 438
11. 33, 57, 59, 188, 264, 316, 387
*
12. 51, 52, 56, 57, 59, 188, 234, 316, 331, 340,
387
13. 51, 52, 54, 56, 57, 59, 60, 188, 193, 229,
303, 316, 331, 373, 387
14. 51, 56, 57, 59, 60, 242, 247, 264, 354, 421
15. 51, 52, 54, 56, 57, 59, 247, 331, 345, 370,
429
16. 33, 51, 52, 54, 56, 57, 59, 60, 101, 113,
116, 117, 132, 160, 176, 181, 193, 194, 229,
252, 255, 258, 303, 331, 344, 352, 370, 373,
378, 433, 438
17. 51, 56, 57, 59, 60, 242, 247, 289, 344, 354,
421, 438
18. 33, 51, 54, 56, 57, 59, 101, 144, 194, 226,
243, 247, 252, 289, 344, 345, 352, 370, 373,
433
19. 1, 3, 4, 5, 6, 7, 8
22, 23, 25, 26, 27,
36, 41, 42, 43, 44,
61, 62, 63, 64, 65,
74, 75, 76, 77, 78,
85, 86, 87, 88, 89,
110, 118, 120, 121,
135, 136, 137, 138,
148, 149, 150, 151,
162, 163, 172, 173,
205, 206, 210. 212,
222, 223, 224, 225,
241, 250, 251, 254,
270, 272, 277, 278,
9,
28,
45,
66,
79,
90,
122
139
153
187
213
230
263
280
,
j
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,
a
,
>
,
10,
29,
46,
67,
80,
92,
123
140
154
189
216
231
266
282
11
31
50
68
81
93
,
j
>
,
>
,
>
>
, 12
, 32
, 53
, 69
, 82
, 95
124,
143,
156,
190,
218,
235,
267,
294,
, 15
, 34
, 55
, 72
, 83
,
,
,
,
,
, 102
3.28
146
.158
191
219
236
268
295
,
»
,
,
,
,
,
5
20,
35,
58,
73,
84 ,
, 108,
129
147
159
199
220
239
269
296
,
,
,
,
,
,
,
,
-3-
-------
297, 298, 301, 302, 305, 306, 307, 309, 310,
311, 312, 313, 314, 315, 317, 321, 3233 324,
325, 326, 327, 328, 329, 330, 333, 334, 335,
336, 337, 3^1, 343, 3'I7, 348, 3495 350, 355,
356, 359, 362, 364, 366, 368, 376, 377, 379;
382, 383, 384, 385, 386, 388, 389, 394, 396,
398, 403, 407, 408, 409, 412, 417, 4l8, 419,
422, 428, 432, 435
20. 2, 3, 17, 18, 19, 21, 24, 28, 37, 39, 40, 423
48S 70, 71, 81, 82, 83, 84, 85, 86, 87, 88,
. 89, 91, 96, 97, 98, 99, 104,, 105, 106, 109,
110, 111, 112, 119, 123, 124, 125, 130, 133,
141, 155, 157, 163, 164, 166, 167, 163, 169,
170, 171, 172, 173, 177, 178, 179, 180, 182,
183, 184, 185, 186, 192, 193, 196, 197, 201,
202, 203, 204, 205, 207, 208, 209, 214, 215,
219, 220, 221, 227, 232, 237, 240, 245, 248,
249, 256, 257, 271, 273, 278, 279, 281, 282,
283, 284, 285, 288, 299. 300, 301, 304, 305,
308, 312, 318, 319, 320, 332, 342, 352, 353,
356, 357, 359, 360, 361, 363, 364, 365, 366,
367, 368, 371, 379, 380, 381, 390, 391, 392,
393, 395, 396, 397, 398, 399, 400, 401, 402,
403, 404, 405, 406, 407, 408, 409, 410, 411,
413, 4l4, 415, 4l6, 4l8, 419, 420, 421, 423,
424, 425, 426, 427, 431, 432, 434, 437, 439
B. Techniques
Aerodynamic Techniques - 144
Airphoto Analysis - 12, 17, 18, 19, 20, 21, 30,
101, 194, 211, 244, 280, 308, 315, 334, 335,
337, 428, 435
Bottom Coring - 134, 230, 263
Data Processing - 1, 2, 3, 4, 5, 6, 7, 8, 9, 10,
11, 12, 13, 14, 15, 16, 17, 18, 19, 20, 21,
22, 23, 24, 25, 26, 27, 28, 29, 31, 32, 33,
34, 35, 36, 37, 38, 39, 40, 41, 42, 43, 44,
45, 46, 47, 48, 49, 50, 51, 52, 53, 54, 55,
56, 57, 58, 59, 60, 61, 62, 63, 64, 65, 66,
67, 68, 69, 70} 71, 72, 73, 74, 75, 76, 77,
78, 79, 80, 81, 82, 83, 84, 85, 86, 87, 88,
89, 90, 91, 92, 93, 94, 95, 96, 97, 98, 99,
102, 103, 104, 105, 106, 107, 109, 110, 111,
-------
112, 113, 114, 115, 116, 117, 118, 119, 120,
121, 122, 123, 124, 125, 126, 127, 128, 129,
130, 131, 132, 133, 134, 135, 136, 137, 138,
139, 140, 142, 1*13, 144, 146, 147, 148, 149,
150, 151, 152, 153, 154, 155, 156, 157, 158,
159, 160, 161, 164, 165, 166, 167, 168, 169,
170, 171, 172, 173, 174, 176, 177, 178, 179,
180, 181, 182, 184, 185, 187, 189, 190, 191,
192, 193, 195, 196, 197, 199, 201, 203, 204,
205, 206, 207, 208, 209, 210, 211, 213, 214,
215, 217, 218, 219, 220, 221, 223, 224, 225,
226, 227, 228, 230, 231, 232, 233, 234, 235,
236, 237, 238, 239, 240, 24l, 243, 244, 245,
246, 248, 249, 251, 253, 254, 255, 256, 257,
258, 259, 260, 26l, 262, 263, 264, 265, 266,
267, 268, 270, 271, 272, 273, 277, 278, 279,
280, 281, 282, 283, 284, 285, 286, 287, 288,
289, 290, 292, 293, 294, 295, 296, 297, 298,
299, 300, 301, 302, 303, 304, 305, 306, 308,
309, 310, 311, 312, 313, 314, 315, 316, 317,
318, 319, 320, 322, 323, 324, 425, 3263 327..
328, 329, 330, 331, 332, 333, 334, 335, 336,
337, 340, 341, 342, 343, 344, 345, 346, 349,
350, 351, 352, 354, 355, 356, 357, 358, 359,
360, 361, 362, 363, 364, 365, 366, 367, 368,
369, 371, 372, 373, 374, 375, 376, 377, 379,
380, 381, 383, 384, 385, 386, 389, 390, 391,
392, 393, 394, 395, 396, 397, 398, 399, 400,
401, 402, 403, 404, 405, 406, 4075 408, 409-
410, 411, 412, 413, 414, 4i5, 4l6, 417, 4l8,
419, 420, 421, 423, 424, 425, 426, 427, 423,
429, 430, 431, 432, 434, 435, 437, 438, 439
Dye Patterns - 8, 199, 260, 261, 274, 275, 276, 291,
293, 303, 370
Echo Profiles - 5, l6l, 339, 340, 354, 389
Heat Energy Standard - 6, 144, 328
Infrared Sensing - 101, 165, 194, 222, 244, 28o,
315, 428, 430
Mathematical Models - 10, 25, 31, 33, 35, 38, 127,
137, 138, 140, 141, 142, 151, 153, 162, 163,
183, 241, 250, 255, 261, 267, 268, 270, 291,
293, 294, 296, 297, 306, 307, 314, 321, 342,
343, 344, 345, 347, 348, 351, 377, 382
-5-
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Modified Current and Wave - 375
Observation - 1, 2, 3, 4, 6, 8, 10, 11, 12, 13, I1*,
15, 16, 17, 18, 19, 20, 21, 22, 24, 26, 28, 30,
32, 33, 34, 35, 36, 37, 39, 40, 41, 42, 43, 44,
46, 47, 48, 51, 52, 53, 54, 55, 56, 57, 58, 59,
60, 61, 62, 63, 64, 65, 66, 67, 68, 69, 70, 71,
72, 73, 745 75, 76, 77, 78, 79, 80, 8l, 82, 83,
84, 85, 86, 87, 88, 89, 90, 91, 94, 96, 97, 98,
99, 102, 103, 104, 105, 106, 107, 109, 110, 111,
112, 113, 114, 115, 116, 117, 118, 119, 120, 121,
122, 123, 124, 125, 126, 128, 129, 130, 131, 132,
133, 134, 135, 136, 137, 138, 139, 140, 143, 144,
146, 148, 149, 151, 152, 151, 155, 156, 157, 158,
159, 160, 163, 164, 166, 167, 168, 169, 170, 171,
172, 173, 174, 175, 176, 177, 178, 179, 180, l8l,
182, 183, 184, 185, 186, 188, 189, 190, 191, 192,
193, 196, 197, 199, 200, 201, 202, 203, 205, 206,
207, 208, 209, 210, 211, 213, 214, 215, 217, 219,
221, 223, 224, 225, 226, 227, 228, 230, 232, 233,
234, 235, 236, 237, 238, 239, 243, 245, 246, 24",
248, 249, 250, 255, 256, 257, 258, 259, 260, 261,
262, 265, 266, 267, 268, 269, 271, 272, 273, 275,
276, 277, 278, 279, 280, 281, 282, 283, 284, 285,
286, 287, 288, 289, 290, 292, 299, 300, 303, 304,
305, 308, 309, 310, 311, 312, 313, 314, 315, 318,
319, 320, 322, 324, 325, 327, 332, 333, 334, 335,
336, 337, 339, 340, 342, 345, 346, 3^8, 3^9, 351
352, 353, 354, 355, 356, 357, 358, 359, 360, 361,
362, 363, 364, 365, 366, 367, 368, 369, 371, 372,
372, 374, 377, 378, 379, 380, 381, 383, 384, 385,
386, 389, 390, 391, 392, 394, 395, 396, 397, 398,
399, 400, 401, 402, 403, 404, 405, 406, 407, 408,
409, 410, 411, 412, 413, 4l4, 415, 416, 417, 418,
419, 420, 422, 423, 424, 425, 426, 427, 430, 432,
433, 435, 437, 439
Radar Analysis - 223
Radiation Analysis - 145, 188, 328
Sample Collection - 1, 2, 3, 4, 5, 6, 8, 9, 11, 12,
13, 14, 15, 16, 22, 26, 28, 30, 31, 32, 33, 34,
35, 36, 39, 40, 42, 43, 44, 46, 47, 48, 50, 51,
52, 53, 54, 55, 56, 57, 58, 59, 60, 6l, 62, 63,
64, 65, 66, 67, 68, 69, 70, 71, 8l, 82, 83, 84,
85, 86, 87, 88, 89, 90, 93, 96, 100, 102, 103,
105, 107, 108, 109, 111, 112, 113, 114, 118, 119,
-------
120, 121, 122, 123, 127, 129, 130, 132, 133,
134, 135, 136, 137, 138, 139, 1*10, 142, 143,
146, 148, 150, 151, 152, 15^, 156, 158, 159,
160, 161, 163, 164, 165, 167, 169, 170, 171,
173, 174, 1763 178, 179, 181, 182, 183, 185,
186, 188, 189, 191, 193, 195, 196, 201, 203,
205, 206, 207, 208, 209, 210S 211, 213, 214,
215, 217, 219, 221, 225, 227, 228, 229, 230,
231, 232, 235, 236, 237, 238, 243, 244, 245,
246, 248S 249, 251, 252, 255, 256, 257, 258,
259, 260, 261, 262, 263, 264, 265, 266, 267,
268, 2695 2703 27-1, 272, 273, 279, 280, 28l,
282, 283, 284, 285, 286, 287, 288, 290, 292,
293, 297, 303, 305, 308, 309, 310, 311, 312,
313, 314, 315, 316, 317, 318, 319, 320, 322,
3235 324, 325, 326, 328, 331, 333, 336, 339,
340, 342, 343, 344, 349, 351, 352, 353, 355,
356, 357, 359, 360, 361, 363, 364, 365, 366,
367, 369, 371, 372, 373, 374, 376, 377, 379,
380, 381, 383, 384, 385, 386, 387, 388, 389,
390, 391, 392, 395, 396, 397, 398, 399, 400,
401, 402, 403, 404, 405, 406, 410, 411, 412,
413. 414, 415, 4l6, 417, 4l8, 419, 420, 421,
423, 424, 425, 426, 427, 428, 430, 431, 432,
436, 437, 438, 439
Seismic Profiling - 112, 207, 219, 253, 308, 354
Side Scan Sonar - l6l, 354
Sp. Cross Spectral Analysis - 198, 242
Written Survey - 350
X-Ray Analysis - 37, 338
C, Instrument at i on
Altitude » 34, 335, 337
Bottom Samplers - 2, 10, 47, 96, 98, 107, 108, 134,
176, 213, 228, 229, 230, 231, 235, 251, 252,
259, 263, 265, 281, 282, 283, 338, 339, 340,
373, 374, 375, 387, 388, 389, 395, 397, 399,
400, 401 421, 436
-7-
-------
Chemical Analyzers - 131, 188, 213, 241, 259, 262,
281, 282, 283, 370
Conductance - 10, 51, 52, 53, 54, 55, 56, 57, 58,
59, 60, 6l, 62, 63, 64, 65, 66, 67, 68, 204,
264, 383
Depth (fathometer) - 2, 6, 8, 14, 15, 16, 26, 33, 44,
48, 51, 52, 53, 54, 55, 56, 57, 58, 59, 60, 61,
62, 63, 64, 65, 66, 67, 68, 69, 70, 71, 81, 82,
83, 84, 85, 86, 87, 93, 107, 110, 118, 119, 120,
121, 122, 123, 124, 129, 132, 134, 140, 148, 149,
150, 151, 152, 158, 159, 163, 173, 174, 175, 178,
185, 186, 187, 206, 213, 219, 227, 236, 237, 239,
246, 251, 255, 259, 261, 263, 267, 268, 28l, 282,
283, 289, 309, 312, 319, 320, 321, 325, 329, 336,
339, 342, 349, 358, 366, 367, 368, 374, 376, 377,
380, 383, 391, 392, 394, 395, 396, 397, 398, 399,
400, 401, 402, 406, 411, 414, 418, 423, 424, 425,
426, 427, 433, 436, 439
Direction - 2, 4, 10, 11, 13, 14, 16, 25, 26, 38, 40,
43, 44, 70, 71, 81, 82, 83, 84, 85, 86, 87, 91,
102, 103, 107, 119, 120, 121, 122, 123, 132, 135,
136, 137, 138, 139, 142, 143, 149, 158, l605 164,
174, 183, 188, 189, 191, 194, 199, 200, 203, 204,
206, 210, 213, 217, 219, 224, 225, 234, 238, 239,
243, 244, 245, 247, 250, 254, 259, 260, 26l, 262,
266, 272, 275, 281, 282, 283, 287, 290, 293, 294,
295, 297, 303, 305, 306, 309, 311, 312, 313, 317,
319, 320, 322, 323, 324, 330, 339, 34l, 343, 344,
345, 348, 349, 351, 353, 355, 366, 367, 372, 380,
382, 384, 391, 392, 394, 395, 396, 397, 398, 399..
400, 401, 402, 403, 404, 405, 406, 410, 411, 4l3,
414, 4jt6, 417, 422, 423, 424, 425, 426, 427, 429,
430, 431
Duration - 2, 42, 70, 71, 119, 187, 194, 210, 213,
224, 272, 281, 282, 283, 290, 297, 313, 319, 320,
336, 395, 397, 399, 400, 401, 402, 406, 431
Dye Readers - 107, 199, 260, 26l, 276, 291, 293
Echo Sounders - 5, 340
Energy - 46, 144, 328, 438
Pluorometers - 107, 26l, 274, 275
-8-
-------
Light - 27, 35, 40, 145, 186, 219, 259, 281, 282,
283, 316, 438
Moisture (evap. hum.) - 8, 34, 41, 43, 44, 46, 96, 98,
144, 150, 213, 219, 223, 224, 225, 227, 259, 281,
282, 283, 287, 295, 309, 311, 314, 317, 369, 384,
386
Photography - 48, 173, 185, 211, 237
Precipitation - 10, 11, 25, 26, 42, 44, 45, 100, 119,
129, 132, 142, 146, 150, 158, 189, 191, 193, 203,
206, 213, 217, 219, 223, 224, 225, 238, 245, 259,
266, 281, 282, 283, 295, 309, 312, 323, 324, 341,
352, 373, 384, 396, 404, 405, 410, 413, 4l6, 417,
423, 424, 425, 426, 427, 431
Pressure -- 25, 44, 136, 144, 210, 213, 219, 247, 294,
297, 309, 344, 372, 381
Radar Scanning - 223
Radiometers - 35, 145, 328, 384
Remote Sensing - 101, 194, 213, 308
Rock Stress - 48, 173, 185, 227, 237, 308, 367, 391,
393, 439
Seismic Testers - 112, 207, 253, 308, 354, 384
Snow Depth (ice) - 22, 32, 36, 89, 90, 120, 213, 223,
225, 226, 310, 335, 337, 384, 385
Sonar - l6l, 354
Spectrometer - 198, 204, 242
Thermal - 1, 3, 4, 5, 6, 8, 9, 10, 11, 12, 14, 34,
36, 43, 44, 50, 51, 52, 53, 54, 55, 56, 57, 58,
59, 60, 61, 62, 63, 64, 65, 66, 67, 68, 88, 101,
132, 136, 137, 139, 140, 144, 154, 156, 163, 165,
188, 189, 191, 193, 194, 195, 213, 217, 219, 222,
224, 225, 236, 241, 244, 259, 261, 262, 264, 266,
270, 272, 280, 281, 282, 283, 286, 290, 292, 297,
303, 309, 310, 312, 313, 315, 317, 322, 323, 324,
325, 326, 327, 328, 329, 330, 331, 336, 343, 345,
369, 372, 376, 377, 382, 383, 384, 386, 395, 396,
397, 399, 400, 401, 403, 407, 408, 409, 412, 415,
417, 428, 429, 430, 438
.9.
-------
Turbldimeters (secchi) - 13, 51, 52, 53, 54, 55, 56, 57,
58. 59, 60, 61, 62, 63, 64, 65, 66, 67, 68, 178,
188, 217, 219, 220, 221, 259, 264, 28l, 282, 283,
286, 328, 383, 403
Underwater TV - 340
Velocity - 2, 4, 8, 10, 11, 13, I1*, 16, 26, 38, 40, 43,
44, 81, 82, 83, 84, 85, 86, 87, 91, 102, 103, 107,
119, 120, 121, 122, 123, 132, 135, 136, 137, 138,
139, 143, 149, 158, 160, 164, 174, 183, 188, 189,
191, 194, 199, 203, 204, 206, 210, 213, 217, 219,
224, 225, 234, 235, 238, 239, 243, 244, 245, 247,
250, 254, 259, 260, 261, 262, 266, 272, 275, 281,
282, 283, 290, 293, 294, 295, 297, 303, 305, 306,
309, 311, 313, 317, 319, 320, 322, 323, 324, 339,
343, 344, 345, 348, 349, 351, 352, 355, 366, 367,
372, 376, 380, 382, 384, 391, 392, 394, 396, 398,
403, 404, 405, 410, 411, 413, 4l4, 4l6, 417, 423,
424, 425, 426, 427, 429, 430, 431
Volume Plow - 2, 13, 14, 26, 31, 44, 70, 71, 81, 82,
83, 84, 85, 86, 87, 91, 102. 103, 119, 120, 121,
122, 123, 124, 132, 136, 138, 139, 140, 143, 146,
148, 149, 150, 151, 158, 160, 178, 183, 187, 189,
191, 196, 203, 206, 211, 217, 219, 220, 238, 239,
245, 248, 259, 268, 272, 281, 282, 283, 284, 292,
295, 303, 305, 309, 319, 320, 323, 324, 341, 342,
352, 366, 367, 369, 376, 377, 380, 383, 394, 395,
396, 397, 398, 399, 400, 401, 402, 404, 405, 406,
407, 408, 409, 410, 411, 412, 413, 4l4, 415, 4l6,
417, 4l8, 423, 424, 425, 526, 427, 430, 431
X-Radiographs - 338, 354
Parameters
Air-Sea-Evaporation - 4, 26, 44, 45, 46, 119, 120,
121, 122, 144, 150, 153, 212, 213, 224, 309,
311, 312, 314, 317, 341, 369
Air-Sea-Heating-Coolong - 4, 46, 50, 51, 52, 53, 54,
55, 56, 57, 58. 59, 60, 6l, 62, 63, 64, 65, 66,
67, 68, 101, 144, 153, 163, 165, 194, 222, 225,
313, 327, 329, 428, 438
-10-
-------
Air-Sea-Mlxins - 101, 144, 194, 219, 222, 274, 291
Air-Sea-Waves - 2, 4, 23, 38, 92, 109, 136, 138, 174,
188, 189, 191, 213, 219, 265, 272, 323, 375, 429
Air-Sea-Wind Stress - 38, 210, 234, 259, 261,> 370
Air-Sea-Wind Transport - 38, 226, 370
Bottom and Shore-Age - 48, 104, 166, 173, 177, 179,
184, 185, 207, 208, 209, 214, 237, 249, 277, 278,
299, 300, 304, 332, 346, 357, 358, 359, 360, 361,
362, 363, 364, 366, 368, 380, 391, 392, 437
Bottom and Shore-Bathymetry - 231
Bottom and Shore-Erosion - 24, 42, 48, 94, 99, 106,
108, 109, 110, 113, 114, 115, 116, 117, 122, 125,
126, 127, 129, 130, 133, 155, 157, 169, 170, 171,
173, 174, 175, 177, 179, 180, 182, 184, 185, 201,
208, 209, 211, 213, 214, 235, 237, 238, 246, 248,
251, 281, 282, 283, 299, 300, 308, 346, 356, 357,
359, 361, 364, 365, 367, 379, 391, 392, 419, 420,
423, 424, 425, 426, 427, 439
Bottom and Shore-Geochemistry - 213, 229, 231, 235,
281, 282, 283, 354, 387, 389
Bottom and Shore-Geological Formation - 2, 24, 37,
39, 48, 99, 104, 105, 106, 109, 110, 134, 155,
157, 166, 168, 169, 170, 171, 173, 177, 179, 181,
182, 184, 185, 201, 202, 205, 208, 209, 214, 232,
237, 240, 249, 256, 271, 277, 278, 279, 285, 288,
298, 299, 300, 304, 318, 322, 346, 353, 356, 357,
358, 359, 360, 361, 362, 363, 364, 365, 366, 367,
368, 371, 379, 380, 381, 390, 391, 392, 419, 420,
432, 437, 439
Bottom and Shore-Geology - 2, 7, 10, 37, 40, 48, 97,
105, 108, 109, 112, 132, 155, 157, 166, 168, 169,
170, 171, 172, 173, 177, 179, 181, 182, 184, 185,
193, 201, 202, 203, 205, 207, 208, 209, 211, 213,
214, 227, 232, 237, 240, 245, 249, 256, 271, 273,
277, 278, 279, 285, 288, 299, 300, 304, 305, 318,
332, 346, 353, 356, 357, 359, 360, 361, 363, 364,
365, 366, 367, 371, 379, 380, 381, 390, 391, 392,
396, 415, 417, 419, 420, 423, 424, 425, 426, 427,
432, 437
-11-
-------
Bottom and Shore-Materials - 5, 14, 24, 48, 49, 94,
96, 98, 99, 104, 106, 155, 157, 161, 167, 173,
176, 177, 179, 180, 185, 197, 202, 208, 213, 219,
227, 228, 229, 230, 231, 235, 236, 237, 241, 248,
251, 252, 258, 263, 273, 277, 278, 281, 282, 283,
287, 299, 300, 338, 339, 346, 364, 367, 373, 374,
375, 388, 389, 391, 392, 412, 436, 439
Bottom and Shore-Paleontology and Palynology - 37, 43,
173, 182, 185, 207, 208, 237, 252, 256, 267
Bottom and Shore-Particle Distribution (topography) -
39, 94, 96, 98, 99, 105, 107, 108, 134, l6l, 167,
176, 201, 213, 219, 228, 229, 231, 232, 235, 248,
251, 256, 258, 271, 277, 279, 285, 287, 288, 318,
338, 340, 353, 364, 371, 373, 375, 381, 387, 388,
389, 390, 436
Bottom and Shore-Physiography - 91, 97, 169, 170, 171,
182, 256, 271, 279, 285, 288, 318, 353, 35^, 371,
381, 390, 398, 439
Bottom and Shore-Properties and Structure -• 5, 14, 39,
48, 94, 96, 98, 99, 105, 107, HO, 13^, 155, 157,
161, 167, 173, 174, 176, 179, 180, 184, 185, 197,
201, 202, 207, 208, 213, 219, 227, 228, 229, 230,
232, 233, 235, 237, 246, 248, 251, 254, 256, 258,
263, 265, 271, 273, 277, 278, 279, 281, 282, 283,
285, 288, 299, 300, 318, 338, 339, 340, 346, 353,
356, 360, 364, 367, 371, 373, 374, 379, 381, 387,
388, 389, 390, 391, 392, 419, 420, 436, 437, 439
Bottom and Shore-Rock Faults and Stress - 37, 48, 112,
173, 185, 227, 237, 273, 308, 363, 367, 381, 437
Bottom and Shore - Sedimentation - 2, 5, 14, 48, 107,
134, 161, 167, 173, 185, 213, 219, 220, 228, 22°,
230, 231, 235, 237, 248, 251, 252, 253, 338, 339,
340, 354, 367, 373, 374, 387, 388, 389, 395, 397,
399, 400, 401, 436
Bottom and Shore-Seismlcs - 219, 384
Bottom and Shore- Shore Processes - 30, 49, 92, 94,
99, 107, 108, 109, HO, 111, 113, 114, 115, 116,
117, 125, 126, 127, 130, 133, 137, 175, 180, 187,
197, 202, 207, 213, 219, 224, 248, 258, 259, 273,
278, 281, 282, 283, 287, 301, 357, 360, 361, 373,
375, 388, 391, 392, 423, 424, 425, 426, 4273 434,
436
-12-
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Bottom and Shore-Siltation - 14, 107, 134, 207, 213,
219, 230, 235, 251, 302, 340, 389
Bottom and Shore-Stratification - 5, 37, 39, 109,
167, 169, 170, 171, 179, 181, 182, 202, 208, 213,
219, 227, 230, 232, 235, 248, 249, 253, 278, 279,
285, 287, 288, 299, 300, 318, 346, 353, 371, 381,
389, 390
Bottom and Shore-X-Radiographs - 252, 338
Dynamics-Color - 188, 189, 191, 204, 221, 323, 324,
383, 412
Dynamics-Currents - 10, 14, 16, 23, 92, 102, 103, 119,
123, 124, 132, 136, 137, 138, 139, 140, 142, 143,
165, 174, 198, 200, 204, 210, 213, 219, 233, 234,
235, 243, 254, 259, 261, 262, 265, 275, 280, 281,
282, 283, 290, 291, 294, 298, 303, 312, 215, 322,
339, 343, 344, 345, 3^7, 351, 355, 370, 375, 398,
403, 422, 429, 430
Dynamics-Diffusion - 14, 16, 92, 101, 135, 138, 140,
194, 199, 213, 219, 259, 275, 276, 280, 281, 282,
283, 293, 298, 303, 312, 315, 430
Dynamics-Discharge Flow - 26, 31, 40, 44, 81, 82, 83,
84, 85, 86, 87, 119, 121, 122, 123, 160, 178, 183,
206, 245, 292, 305, 306, 319, 320, 332, 352, 364,
369, 333, 396, 404, 405, 407, 4o8, 409, 410, 413,
415, 416, 431
Dynamics- Diversions - 69, 119, 120, 121, 122, 218,
239, 309, 342, 367, 394, 434
Dynamics-Flushing (exchange) - 259
Dynamlcs-Groundwater - 44, 92, 132, 190, 193, 196,
203, 206, 219, 227, 257, 259, 268, 352, 395,
397, 399, 400, 401, 404, 405, 4lO, 413, 4l6,
417, 423, 424, 425, 426, 427
Dynamics-Internal Waves - 136, 213, 219, 244, 272, 303
Dynamics-Light Penetration - 13, 27, 51, 52, 53, 54,
55, 56, 57, 58, 59, 60, 61, 62, 63, 64, 65, 66,
67, 68, 189, 191, 217, 219, 220, 221, 259, 264,
281, 282, 283, 286, 323, 324, 327, 383, 403, 438
-13-
-------
Dynamics-Mixing (internal) - 14, 23, 47, 213, 219, 259,
262, 272, 280, 290, 303, 315, 430
Dynamics-Odor - 13
Dynamics-Oscillations - 15, 23, 183, 189, 191, 198,
213, 261, 272, 298, 321, 422
Dynamics-Outflow Volume (inflow) - 14, 26, 31, 40,
44, 70, 71, 119, 120, 121, 122, 123, 124, 146,
148, 149, 150, 160, 183, 186, 206, 212, 219, 239,
240, 248, 284, 305, 306, 319, 320, 366, 377, 380,
393, 394, 396, 397, 399, 400, 401, 402, 406
Dynamics-Runoff (drainage) - 2, 8, 14, 26, 40, 42, 44 ,
69, 70, 71, 81, 82, 83, 84, 85, 86, 87, 91, 119,
120, 132, 149, 150, 160, 163, 178, 196, 203, 212,
219, 220, 227, 238, 239, 259, 278, 28l, 282, 283,
298, 319, 320, 341, 342, 352, 394, 395, 396, 397,
399, 400, 401, 402, 404, 405, 406, 410, 411, 412,
4l33 414, 415, 416, 417, 4l8, 423, 424, 425, 426.
427, 431
Dynamics-Suspended Solids - 28, 178, 241, 286, 342, 383
Dynamics -Temperature Gradients - 5, 8, 9, 47, 51, 52, 53
54, 55, 56, 57, 58, 59, 60, 6l, 62, 63, 64, 65, 66,
67, 68, 132, 136, 138, 140, 141, 154, 163, 195, 213,
236, 259, 261, 322, 323, 324, 327, 329, 330, 331,
376, 377
Dynamics-Thermal - 1, 5, 6, 11, 12, 14, 43, 50, 92, 139,
143, 153, 156, 165, 189, 191, 194, 195, 204, 206;
213, 217, 219, 225, 226, 24l, 244, 259, 26l, 262,
264, 266, 2705 272, 280, 281, 282, 283, 286, 292,
295, 312, 315, 317, 322, 323, 324, 327, 328, 345;
369, 384, 386, 395, 397, 399, 400, 401, 403, 4l2,
415, 417
Dynamics-Thermal Bar - 10, 137, 154, 195, 213, 219,
269, 325, 326, 327, 331
Dynamics-Transport (volume) - 16 , 92, 178, 259, 274,
281, 282, 283, 291, 319, 320, 339, 34l, 376, 393,
, 4l4
Dynamics-Turbulence - 135, 213, 219, 275, 281, 282,
283, 327
-14-
-------
Ice-Snow-Albedo - 36, 310
Ice-Snow-Buildup and Decay - 3, 11, 17, 18, 19, 20, 21,
22, 32, 88, 89, 90, 120, 128, 154, 205, 213, 223,
224, 225, 310, 333, 334, 335, 336, 337, 384, 385,
432, 435
Ice-Snow-Occurrence - 3, 5, 11, 17, 18, 19, 20, 21, 22,
32, 33, 36, 88, 89, 90, 120, 154, 205, 213, 2?3,
224, 225, 226, 245, 266, 268, 289, 307, 310, 312,
333, 334, 335, 336, 337, 378, 384, 385, 432, 433,
435
Ice-Snow-Physical Properties - 3, 11, 22, 32, 36, 88,
89, 90, 128, 205/213, 224, 225, 226, 266, 310,
333, 334, 335, 336, 337, 435
Ice-Snow-Thickness and Density - 3, 11, 17, 18, 19, 20,
21, 22, 32, 33, 36, 88, 89, 90, 128, 154, 205, 213,
224, 225, 289, 310, 333, 334, 335, 336, 337, 384,
385, 432, 435
Meteorology-Air Currents - 13, 247, 262, 297, 382
Meteorology-Barometric Pressure - 136, 189, 191, 297,
305, 309, 314, 344, 372
Meteorology-Climatology - 7, 8, 10, 11, 31, 34, 42,
92. 102, 103, 119, 120, 162, 163, 200, 219, 223,
224, 225, 254, 266, 279, 286, 295, 298, 307, 311.
3125 328, 349, 398, 372, 382, 417, 433
Meteorology-Cloud Formations - 188, 189, 191, 223, 22*!,
247, 297, 323, 324, 378, 384
Meteorology-Convection - 297, 378
Meteorology-Coriolls Force - 137
Meteorology-Gravatational Force - 8, 15, 145, 164
Meteorology-Humidity - 34, 13, 188, 189, 191, 21*5, 305,
317, 323, 324, 384, 386
Meteorology-Lighting - 223
Meteorology-Observations - 10, 188
Meteorology-Particulates ~ 223
-15-
-------
Meteorology-Precipitation - 10, 11, 26, 34, 41, 42, 44,
45, 69, 92, 119, 120, 121, 122, 129, 132, 144, 146,
148, 149, 150, 153, 193, 203, 212, 213, 215, 219,
225, 239, 245, 259, 266, 28l3 282, 283, 295, 305,
309, 312, 341, 352, 372, 384, 386, 394, 395, 397,
399, ^00, 401, 417, 423, 424, 425, 426, 42?
Meteorology-Radiation - 35, 188, 189, 191, 311, 316,
323, 324, 328, 384, 438
Meteorology-Temperature - 6, 10, 43, 188, 189, 191,
193, 204, 215, 223, 224, 226, 266, 292, 305, 313,
317, 323, 324, 355, 372, 382, 384
Meteorology-Wind Force - 23, 25, 38, 210, 217, 219,
225, 234, 247, 294, 312, 382, 385, 430
Meteorology-Wind Stress - 25, 38, 210, 247, 259, 321 382
Meteorology-Wind Turbulence - 210, 247, 382
Meteorology-Wind Velocity and Direction - 11, 16, 43,
92, 102, 103, 136, 137, 138, 174, 189, 191, 204,
225, 235, 238, 250, 272, 295, 303, 305, 309, 311,
313, 317, 323, 324, 336, 355, 373, 376, 377, 382,
384, 430
Water Levels-Depth - 118, 137, 158, 263, 265, 267, 355
Water Levels-Lake Levels - 8, 15, 23, 44, 69, 70, 71, 72
73, 74, 75, 76, 77, 78, 79, 80, 92, 93, 110, 118,
119, 120, 121, 122, 123, 124, 129, 132, 137, 148,
149, 150, 151, 152, 158, 159, 174, 187, 198, 206,
212, 213, 218, 219, 239, 242, 246, 255, 259, 261,
267, 2,^8, 281, 282, 283, 298, 309, 357, 358, 3603
361, 366, 367, 376, 380, 383, 394, 395, 397, 398,
399, 400, 401, 402, 406, 4l8, 434
Water Levels-Seiches - 23, 92, 152, 198, 213, 348, 398
Water Levels-Tides - 72, 72, 73, 75, 76, 77, 78, 79, 80,
92, 183, 198, 213, 349
Water Mass-Dimentional - 2, 14, 26, 28, 29, 49, 95, l."9,
132, 160, 163, 192, 213, 298, 332, 336, 398, 407,
408, 409, 417, 4l8
Water Mass-Observations - 26, 95, 160, 188, 321, 398
-16-
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Water Mass-Physical (location) - 2, 7, 26, 47, 95, 160,
190, 192, 213, 298, 332, 398, 403, 417, 429
Water Mass-Specific Conductance - 10, 51, 52, 53, 54,
55, 56, 57, 58, 59, 60, 61, 62, 63, 64, 65, 66, 67,
68, 100, 188, 204, 264, 323, 324, 383
Water Surface-Observations - 188, 274
Water Surface=Physical - 7, 204
-17-
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III. ABSTRACTS
The location of those papers not found in Buffalo
and available through the Great Lakes Lab are given in
parenthesis at the end of the abstract.
1. Acres, H. G. 1970. Effects of thermal inputs to Lake
Ontario, 1968-2000. Niagara Falls, Ontario. 81 p.
Annual evaporation from the surface of Lake Ontario,
resulting from man-made heat input, is expected to
increase from 0.04? inches in 1968 to 0.14 inches in
1980 and 0.64 inches in 2000. The total increased
evaporation from the surface of the Great Lakes over
the natural state is estimated to be 0.1600 cfs by
the year 2000. (Canada Centre for Inland Waters).
2. Adams, C. C. 1927. General description of Oneida Lake.
Roosevelt Wild Life Annuals. 1(3 and 4):247-248.
A description of the dimensional and physical charac-
teristics of Oneida Lake with reference to location,
dimention, depth, volume, waves, sediments, geological
formations, glacial and post glacial deposits and
drainage area.
3. Allen, W. T. R. 1964. Break-up and freeze-up dates
in Canada. Canadian Dept. Transport, Meteorological
Branch. Clr. 4ll6, Ice 17. 301 p.
As the result of a survey of meteorological stations
made in 1956 to obtain historical records of the dates
of break-up and freeze-up of rivers and lakes in
CAnada; and the establishment of a continuing program
at the stations to report these phenomena; the Meteoro-
logical Branch published, in 1959, Circular 3156, ICE-2,
"Break-up and Freeze-up Dates of Rivers and Lakes in
Canada." This circular contained listings of break-up
and freeze-up dates for 87 rivers and 113 lakes, bays
and harbours, up to break-up 1958.
Five additional years of records are now available for
the meteorological stations which have been engaged in
observing the break-up and freeze-up of bodies of water
in their vicinity. In addition, historical records,
some quite lengthy, have been obtained for a number of
other locations. This present circular lists all Infor-
mation acquired since the publication of Circular 3156,
up to freeze-up 1963. (Univ. Toronto-Great Lakes Inst.),
-18-
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Anderson, D. V. - See: J. P. Bruce, No. 43.
Anderson, D. V. - See: R. L. Drake, No. 162.
Anderson, D. V. - See: D. H. Matheson, No. 262.
Anderson, D. V. - See: Q. K. Rodgers, No. 328, 329.
Anderson, D. V. - See: R. N. Simpson, No. 3^8, 3^9.
Anderson, D. V. 1959. The effect of a water temperature
discontinuity on wind water interaction. Ontario
Dept. Lands and Forests Research Division. Physics
Research Note No. 3. 2 p., 1 Figure.
The passage of air over a body of water is a more com-
plicated and far-reaching phenomenon than apparent to
casual observation. As the strength of wind increases
from zero and waves are generated in Increasing size,
several phenomena occur. For one, the vertical profile
of the wind over the water is -modified and energy is
transferred to the water which is set in motion bodily,
i.e. in addition to the surface disturbance of the
water, a surface layer is associatively induced into
motion by the wind. Because of the compounded diffi-
culties of making correlative and simultaneous
measurements on the air above and the water below, the
mechanics of the interaction are not at all thoroughly
understood. However, much work is being devoted to
the problem in oceanographlc research, and It is hoped
to do likewise on the Lakes.
One facet of the matter lies in the difference encoun-
tered in the contrasting situation: air at a given
temperature passing over water that is colder than the
air; and over water that is warmer.
The first is termed a stable condition because the
surface layer of air cooled by contact with the colder
water, and therefore, heavier than the air above, tends
to stay near the surface. It is well known that this
cool layer acts as a lubricant on the general body of
wind so that the air above is less affected by contact
with the water and, correspondingly, the cool layer in
contact with the roughened surface of the lake is
slowed down. Therefore, the velocity will vary in the
simplest case from close to zero very near the surface
to the unimpeded maximum several hundred feet above
the water.
-19-
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The stronger the wind, the thinner the layer, for
turbulence in the movement of the air increased by
effects of waves will break down the layer and mix the
cooler air with the warmer above, thereby permitting
an increasing speed of wind and turbulence at the water
surface and allowing a greater drag on the air above.
In consequence of all this, winds of moderate speed with
a given air temperature should produce smaller waves on
water that is colder, than on water that is warmer than
the air, although the evidence on this is not conclusive
(Darbyshire and Darbyshire, 1950). (Univ. Toronto,
Zeology Library).
5. Anderson, D. V. I960. Canadian Great Lakes Research
Program. The Conservationist. August-September.
pp. 2-5.
An article on the Canadian Great Lakes Research Program
initiated by the Ontario Department of Lands and Forests.
Parameters for the years 1959 and I960 include:
Temperature distribution
Ice observations
Echo Sounder bottom sediment survey
Water in the Toronto region of the lake has an average
summer surface temperature of 65°F, while the more
southerly areas were somewhat warmer (70°F average).
6. Anderson, D. V. 1961. A preliminary study of the
energy budget of Lake Ontario. Journal Fish.
Research Board Canada. 18(4): 617-636.
Recent bathythermographic surveys carried out on the
research vessel Port Dauphlne have provided estimates
of the heat content of Lake Ontario and permitted a
preliminary study of its energy budget. The imbalance
between the absorbed sbort wavelength sun and sky
radiation, and the losses due to evaporation, sensible
heat conduction and net long wavelength back radiation
result in heating of lake water from March to August
and cooling from September to October to February. The
peak heat content lags the peak surface temperature by
about one month. The amount of energy advected into
the lake is relatively small compared with other terms
in the energy budget. Thus, energy budget calculations
do not depend upon the accuracy ivith which the water
budget is known. The principal difficulty in applying
present techniques for determination of an energy budget
is lack of meteorological data over the lake surfaces.
-20-
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7. Anderson, D. V. 1964. Geophysical research on the Great
Lakes. Ontario Dept. Lands and Forests. Research
Report Mo. 55. 39 p.
A summary of geophysical research on the Great Lakes,
the major research agencies, problems in physical
limnology, and a discussion of instrumental techniques
and methods. Also included are the various research
fields and projects undertaken, and a proposal for
organization of the geophysical research.
8. Anderson, D. V. 196?a. Diurnal motions of the thermo-
cline of Lake Ontario caused by meteorological and
tidal factors. Ontario Dept. Lands and Forests.
Research Rept. No, 17. 15 p.
Average water temperatures at the summer level of the
thermocline at Toronto reveal correlation with the four-
angles of both sun and moon. Their forms are diurnal
and it is suggested that the solar correlation has super-
Imposed upon a gravitational tidal component a diurnal
meteorological component due to the wind.
9. Anderson, D. V. 1967b. A prolegomenon to the study of
Lake Ontario. Ontario Dept. Lands and Forests,
Research Branch. Report No. 81. 90 p.
This report is the last one of a series describing
limnological investigations started by Dr. Anderson
while he was with the Department of Lands and Forests.
This report presents data collected on surveys of Lake
Ontario from 1955, 1958 and 1959. They are summarized
in charts which will be allowed to speak mainly for
themselves pending comparison with recent data. Four
anomalies in temperature structure are commented upon
and taken as illustrations to shoxv that a physical
research program oriented toward administrative action
would be based, for the present, upon statistical
models. Detailed explanations of motions will not be
easily achieved and may not be necessary in many
practical cases.
10. Anderson, D. V. (Ed.). 1969- The Great Lakes as an
environment. Great Lakes Institute, Univ. Toronto.
Report PR 39. 189 p. + appendices.
Tabulated data for the surface water of Lake Ontario
are presented on: conductivitys dissolved solids and
-21-
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pH. A climatological summary of the Great Lakes Basin
Is included which summaries the data obtained from 110
Canadian and 160 U. S. weather stations located In the
Great Lakes Basin.
Other sections Included weather and temperature and
currents in the Great Lakes, (Canada Centre for Inland
Waters).
11. Anderson3 D. V., J. P. Bruce, U, Sporns and G. K.
Rodgers. 1961. Winter research on Lake Ontario.
Great Lakes Research Division. Publication No. 7.
po. 185-198.
The relationship of meteorological and cftlmatologlcal
factors and water processes are discussed. Water
temperatures, meteorological factors, Ice observations
and storms are discussed.
12. Anderson, D. V. and Y. T. Lanbert. 1959. A synoptic
survey of Lake Ontario in a Canso flying boat.
Ontario Dept. Lands and Forests, Research Division.
Note No. 2. pp. 1-2.
The advantage to this type of survey is that little
variation takes place in climatology (winds, temp., etc.)
during the very brief sampling period. The only dis-
advantage was the necessity for calm lake conditions
for landing. (Univ. Toronto, Zoology Library).
13. Anderson,, D. V. and D. H. Matheson. 196?. Hamilton
Bay - The model of a natural waste treatment reactor
Ontario Dept. Lands and Forests, Research Rept. No.
73. 15 p.
Hamilton Bay covers 11.3 square miles and communicates
with Lake Ontario through a short shipping channel.
All wastes from the city are discharged into the Bay
where, in water averaging 20 feet of depth, they are
subject to active and effective decomposition. Analysis
of the Bay water and Lake water nearby have been made
over 20 years, and during this period the Bay has been
able to cope with the cities wastes. Increased pollution
and reduced detention times now make problemmatical the
stability of the bay as a sewage reactor. Of course,
the reactions are much too complicated yet to be dis-
cussed even qualitatively, and therefore, It is not
possible to defend increased demands on the Bay. In any
case, secondary treatment facilities are now being built.
-22-
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14. Anderson, D. V. and G. K. Rodgers. 1959- The delta of
the Niagara River, Ontario Dept, Lands and Forests.
Physics Research Note No. 5. 4 p., 7 Figures.
Most of the sands and all of the gravels are deposited
within six miles of the mouth of the Niagara River.
This indicates that the momentum of the River along the
bottom is dissipated within the lake in approximately the
same distance, or of the order of 10 miles. Thereafter,
the movement of Niagara River water, while it will remain
more or less en bloc for a much greater distance, must be
controlled by Lake forces. The movement of warmer river
water across the surface of relatively colder Ontario
water is another matter upon which coarse bottom sedi-
ments shed little light since they settle out rapidly.
Assessment of the distribution of silts should be diag-
nostic of such surface flow.
The orientation of the mouth directs the river water
to the north-west and the greatest depths of material
are deposited as shown by the contour lines in Figure
3 in a fan directed to the north-west. But the isodia-
metral lines of Figure 6 show that particles of a given
size are moved further to the north-east than to the
north-west. Superimposed upon the current of the river
there must be a current which on the average is flowing
easterly, and so causes earlier sedimentation. Now
current and other measurements will be necessary to
settle the matter, but in addition to wind-driven
currents another type of flow may be partially res-
ponsible. It was found in the course of other work in
1958 that the flow of xtfarm river water into the Lake
may Induce a coutour flow of colder bottom water from
the Lake toward the shore, a flow which could account
partially for the observed effect as indicated
schematically in Figure 7.
Appeal to Figure 1 shows that the maximum velocity
indicated by fine sand 0.001 inches in diameter (0.02 mm)
is 0.004 mph (0.15 cm/sec., 0.005 ft/sec,). The depths
at the -3.0 contour (Fig. 5)are about 200 feet and the
very slight magnitudes of bottom currents indicated
there, agree with those obtained by dynamic height cal-
culations in the west basin. At the river's mouth,
Station 40-11, the maximum particle size of 0.4 inches
(10 mm) and calculated river flow velocity of 2.5 mph
are in substantial agreement. The flow is approximately
190,000 cfs, and the dimensions of the river mouth are:
width 1,300 ft., maximum depth 63 ft. (Univ. Toronto,
Zoology Library).
-23-
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15. Anderson, D. V. and R. B. Simpson. 196?. The surface
tides of Lake Ontario. Ontario Department of
Lands and Forests. Research Report No. 76. 42 p.
Monthly averages of surface levels at successive hours,
reveal the lunar and solar tides of Lake Ontario. The
relative amplitudes and phases in the eastern, central
and western basins are in accord with theory. It is
suggested that intensive tidal studies will help unravel
puzzles in circulation and that they may be useful in
constructing correlations with seasonal meteorological
changes.
Anderson, S. R. - See: M. K. Thomas, No. 386.
16. Andrews, R. H. G. and S. A. Black. 1968. Diffusion
of Lakeview WPCP effluent in Lake Ontario. Abstract
of paper presented at the llth Conference Great
Lakes Research, Univ. of Wisconsin, Milwaukee.
pp. 28-29.
As part of a general county survey involving the
enlargenent of the Lakeview Water Pollution Control
Plant fi'om 5 to 12 mgd. The project was undertaken to
estimate-- the present and future influence of this waste
efflu'» * upon the water quality at the New Toronto and
Tor« >r o Township Waterworks intakes in Lake Ontario.
Cir- -ent velocity and direction was determined to be
largely a result of wind conditions. Depending upon
wird conditions at a given sample time, varying con-
centrations of Lakeview WPCP effluent could conceivably
reach the water intakes of these areas, however, not in
dangerous concentrations.
17. Archibald, D. C., M. N. Monsinger and T. B. Kilpatrick.
1959. Aerial ice observing and reconnaissance
program in the St. Lawrence River, the Gulf of
the St. Lawrence and the Strait of Belle Isle, 1958.
Department of Transport, Meteorological Branch,
Canada. Circular 3273. 19 p.
This is the second technical report in the series con-
cerning ice conditions observed by aerial ice reconnaiss-
ance conducted by the Meteorological Branch, Department
of Transport. This survey was carried out in cooperation
with the Marine Branch, Department of Transport and the
Geographical Branch, Department of Mines and Technical
Surveys.
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This technical report describes observed ice conditions
with regard to ice coverage, age, topography, puddling,
snow cover, ice of land origin and water features over
the area of the St. Lawrence River, the Gulf of St.
Lawrence and the Strait of Belle Isle during the period
January to June, 1958, inclusive. (Univ. of Toronto,
Zoology Library).
18. Archibald, D. C., M. N. Monsinger and T. B. Kilpatrick.
I960. Aerial sea ice observing and reconnassance -
St. Lawrence River, the Gulf of the St. Lawrence
and coastal waters of Newfoundland, 1959- Depart-
ment of Transport, Meteorological Branch, Canada.
Circular 3417. 99 p.
This is the fifth technical report in the series con-
cerning ice conditions observed by aerial ice reconnaiss-
ance under direction of the Basic Weather Division,
Meteorological Branch, Department of Transport.
This technical report describes observed ice conditions
with regard to ice coverage, age, topography, puddling,
snow cover, ice o- land origin and water features over
the area of the St. Lawrence River, the Gulf of St.
Lawrence and the coastal waters of Newfoundland during
the period from December 21, 1958 to June 24, 1959.
(Univ. of Toronto, Zoology Library).
19. Archibald, D. C., M. N. Monsinger and T. B. Kilpatrick.
196la. Aerial sea ice observing and reconnaissance
St. Lawrence River, the Gulf of the St. Lawrence
and coastal waters of Newfoundland, I960. Depart-
ment of Transport, Meteorological Branch, Canada.
Circular 3465. 101 p.
This is the seventh technical report in the series con-
cerning ice conditions observed by aerial Ice reconnaiss-
ance conducted by the Basic Weather Division,
Meteorological Branch, Department of Transport.
This Is the third annual technical report covering
observed ice conditions in the St. Lawrence River, the
Gulf of St. Lawrence and coastal waters of Newfoundland.
This technical report describes observed ice conditions
with regard to ice coverage, age, topography, puddling,
snow cover, ice of land origin and water features over
the described area during the period December 19, 1959
to June 28, I960. (Univ. of Toronto, Zoology Library).
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0. Archibald, D. C., M. N. Monsinger and T. B. Kilpatrlck.
196lb. Aerial ice observing and reconnaissance -
the Great Lakes, 1961. Department of Transport,
Meteorological Branch, Canada. Circular 3530. 55 p.
This is the ninth technical report in the series con-
cerning the ice conditions observed by aerial ice
reconnaissance conducted by the Meteorological Branch,
Department of Transport.
This technical report describes observed ice conditions
with regard to ice coverage, age, topography, puddling,
snow cover and water features over the area of Lake
Superior, the North Channel, Georgian Bay, Lake Huron,
Lake Erie, Lake Ontario and adjacent waterways, during
the period January to April, 1961, inclusive.
This is the second technical report covering observed
ice conditions in the Great Lakes. (Univ. of Toronto,
Zoology Library).
21. Archibald, D. C., M. N. Monsinger and T. B. Kilpatrick.
1962a. Aerial sea ice observing and reconnaissance
St. Lawrence River, the Gulf of the St. Lawrence and
coastal waters of Newfoundland, 1961. Department of
Transport, Meteorological Branch, Canada. Circular
3591. 157 P.
This is the twelfth technical report in the series con-
cerning ice conditions observed by aerial ice reconaiss-
ance conducted by the Basic Weather Division,
Meteorological Branch, Department of Transport.
This is the fourth annual technical report covering
observed ice conditions in the St. Lawrence River, the
Gulf of St. Lawrence and coastal waters of Newfoundland.
This technical report describes observed ice conditions
with regard to Ice coverage, age, topography, puddling,
snow cover, ice of land origin and water features over
the described area during the period from December 18,
I960, to June 27, 1961. (Univ. of Toronto, Zoology
Library).
22. Archibald, D. C., M. N. Monsinger, T. B. Kilpatrick.
1962b. Aerial ice observing and reconnaissance -
the Great Lakes, 1962. Department of Transport,
Meteorological Branch, Canada. Circular 3772,
Tec. MO. 55 p.
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This is the sixteenth technical report in the series
concerning the ice conditions observed by aerial ice
reconnaissance conducted by the Meteorological Branch,
Department of Transport.
This technical report describes observed ice conditions
with regard to ice coverage, age topography, puddling,
snow cover and water features over the area of Lake
Superior, the North Channel, Georgian Bay, Lake Huron,
Lake Erie, Lake Ontario and adjacent waterways, during
the period December, 1961 to May, 1962, inclusive.
(Univ. of Toronto - Great Lakes Institute).
Armstrong, J. L. - See: S. J. G. Bird, No. 30.
23. Ayers, J. C. 1962. Great Lakes water, their circula-
tion and physical and chemical characteristics.
American Association Advancement Science.
Publication 71: 71-89.
The circulation of water in the Great Lakes involves
surface and subsurface currents, with a seasonal cycle
of verticle circulation superimposed. Current patterns
are determined by wind, flowthrough of drainage water,
rotation of the earth and local influences. Surface
currents lag behind the causative wind by periods
ranging from two hours in shallow water to a day in deep
basins. Current patterns in deep basins apparently
involve energy increments from the winds of the preceed-
ing 10-12 days, with the increments increasing
exponentially in effectiveness with increasing time
prior to the observation day.
Primary physical characteristics of the lake waters
are their "soft water" nature; their seasonal cycles
of turnover, lake levels and precipitation; and their
short period seiches. The lake exhibit a modified
seasonal turnover cycle, wind mixing establishes turn-
over at the end of the fall cooling period and maintains
it throughout the winter until the spring warming period
is established. Cycles of the lake level occur annually
the levels are low in midsummer. Superimposed on the
annual cycles are multiyear cycles of level.
24. Bakewell, R. 1857. Observations on the falls of
Niagara, with reference to the changes which have
taken place and are in progress. American Journal
Science. Ser. 2, 23: 85-95.
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The Niagara Palls and their related erosion rates are
responsible for the formation of the Niagara Gorge.
The harder upper limestone formations are undermined
by the erosion of softer shales and sandstones near the
base of the falls. This causes collapse and subsequent
erosion of the material under the falls. This is thought
to be the mechanism for the gradual formation of the
Niagara Gorge.
Baldwin, A. L. - See: R. C. Bubeck, No. 47.
25. Barrientos, C. S. 1971. An objective method for
forecasting winds over Lake Erie and Lake Ontario.
Abstract of paper presented at the 14th Conference
Great Lakes Research, Toronto, pp. 41-42.
An objective method for forecasting surface winds over
Lake Erie and Lake Ontario has been developed. The
differential data consisted of 1000 mb geostrophic wind
forecasts from the Subsynoptic Advection Model (SAM) for
eight U. S. cities near the two lakes, as well as marine
observations (MOABS) made by anemometer-equipt vessels
during the 1968-69 boating season. Two sets of wind
speed forcast equations were derived by applying a
screening regression technique. The first set of
equations yields wind speed by vectorial addition of
two directional components; the second set yields wind
speed directly. Verification shows that wind speed
forcasts made by combining components are negatively
biased. The resulting operational program is described.
26. Barrows, H» K. and A. H. Horton. 1907. Surface water
supply of Great Lakes and St. Lawrence River
drainages - 1906. U. S. Geological Survey Water
Supply Paper and Irrigation Paper No. 206 (1-6):
1-98.
Precipitation, evaporation, tributary flow, inflow
from the Niagara River and outflow from the St. Lawrence
River all effect the surface water supply of Lake Ontario
and the same parameters affect all the supply of the
Great Lakes System. Each is discussed separately and
then all combined to give the overall picture of effects
on the surface water supply.
Beeton, A. M. - See: J. E. Gannon, No. 176.
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27. Beeton, A. M. 1962. Light penetration in the Great
Lakes. Proceedings 5th Conference Great Lakes
Research, Ann Arbor, Michigan, p. 68-77.
Measurement has been made of incident and subsurface
light intensities at several depths in Lakes Erie,
Michigan, Huron, Ontario and Superior. At least one
study was made of spectral distribution of ambient
irradlence in each of the Lakes. Blue light penetrated
to the greatest depths in Lake Huron, green in Lakes
Superior and Michigan and orange in Lakes Erie and
Ontario. Measurements were made of the changes in
light intensities at several depths from sunrise to
sunset in Lakes Erie and Michigan and Prains Lake, a
small inland lake. The percentage of Incidence
irradience at depth was greatest at sunrise and sunset
in Lake Erie and Prains Lake. The situation occurs
since incidence irradience is shifted toward the red
end of the spectrum at sunrise and sunset. Consequently,
a greater percentage of the incident light was in the
orange region of the spectrum that penetrates deepest in
these lakes. Shorter wavelengths penetrate to greater
depths in Lake Michigan.
28. Beeton, A. M. 1969. Changes in the environment and
the eutrophlcation of the Great Lakes. In:
Eutrophication causes, consequences, correctives.
National Academy of Science, pp. 150-187.
A discussion of environmental changes as a result of
eutrophication of Lake Ontario. Dimensional and flow
volume data are presented for the Niagara River and
general location and dimensions of Lake Ontario.
Suspended solids are also discussed.
29. Beeton, A. M. and D. C. Chandler. 1963. The St.
Lawrence Great Lakes. Limnology in North America.
Univ. of Wisconsin Press, Madison, Wisconsin.
pp. 535-558.
General geographic and dimensional information about
the Great Lakes including Lake Ontario. A history of
Lake research is also presented in this paper.
30. Bird, S. J. G. and J. L. Armstrong. 1970. Scarborough
Bluffs - a recessional study. Proceedings 13th
Conference Great Lakes Research, Buffalo, pp.
187-197.
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The unusual geological formation known as the
Scarborough Bluffs, east of Toronto, has always
been of interest to scientist and layman. The severe
conditions of recession of the summit and erosion of
the toe have become a serious problem. The result is
substancial removal of valuable land, virtually price-
less because of its geographical location. The study
involved research of all available literature, airphoto
analysis and extensive field investigations. All
possible sources of erosion and recession were examined
and evaluated. Ground water was found to be of critical
importance, contrary to many previous theories. The
difficulties and consequences of stabolization are many
and varied.
Black, S. A. - See: R. H. G. Andrews, No. 16.
31. Bolduc, P. A. 1970. The change of water level caused
by the variation of the inflow outflow on Lake
Ontario. Department of Energy, Mines and
Resources, Ottawa. 27 p.
A numerical model was developed which was successful
in analysing the change in water level caused by the
relation of the inflow-outflow of Lake Ontario. It
is planned to study the other causes of variation such
as wind and atmospheric pressure with the same model.
Work will be carried out on the combined effects of
all the causes of variation. On shore meteorological
data will be required as input in the model. (Canada
Centre for Inland Waters).
32. Bolsenga, S. J. 1967a. Great Lakes snow depth pro-
bability charts and tables. U. S. Army Corps of
Engineers, Lake Survey Report RR-5-2. 3** p.
Published information on representative or complete
Great Lakes snow cover conditions in lacking. This
report presents the results of snow depth probability
calculations for selected stations in and near the
Great Lakes basin. These calculations, in tabular
and graphic form, will be valuable to the scientist,
as well as the layman.
All computations are based on snow on the ground data
at the end of each month. The possibility of similar
studies on a weekly or even a daily basis should be
considered so that the frequency and effect of
individual storms might be observed. Ultimately, a
forecasting system for expected depths using given
sets cf projected meteorological conditions should
be developed.
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33. Bolsenga., S. J. 196?b. Snow depth probability in
the Great Lakes basin. Proceedings 10th Conference
Great Lakes Research, pp. 162-170.
Snow depth probability was computed for ^5 stations in
the Great Lakes Basin using data on snow depth at the
end of the month. Probability patterns of snow cover,
for the basin and for each lake region, are presented
using isoline charts, graphs and tables.
For the basin, probability charts indicate marked
increases from the extreme southern to the extreme
northern portion of the basin. For each lake region,
the probable occurrance of selected depths is analysed
using graphs of probability as a function of station
location.
31*. Bolsenga, S. J. 196?c. Total atmospheric water vapor
aloft over the Great Lakes basin. U. S. Army Corps
of Engineers, Lake Survey Report RR 5-3. 20 p.
This report presents the results of a study on the
quantity and distribution of atmospheric water vapor
aloft over the Great Lakes as a part of the Ice and
Snow Research Project. The study was conducted under
the general direction of Dr. L. Bajorunas, Director,
Great Lakes Research Center, U. S. Lake Survey and
Dr. E. W. Marshall, Chief of the Ice and Snow Project.
35. Bolsenga, S. J. 1968a. Great Lakes solar attitude
charts and tables. U. S. Army Corps of Engineers,
Lake Survey Report TT 5-^. 110 p.
A knowledge of the solar altitude is necessary
for shortwave balance studies and is also used in
daylight duration and sunrise-sunset determinations.
This report presents detailed electronic computer
calculations of solar altitudes for the entire Great
Lakes basin. Using standard astronomical equations,
solar altitude was computed as a function of the
latitude, solar declination and true solar time.
An analysis of solar altitudes and related quantities
at the summer and winter solstices indicates wide
variation from the northern to the southern portion
of the basin.
36. Bolsenga, S. J. 1968b. Total albedo of Great Lakes
Ice. U. S. Lake Survey, Detroit, Michigan.
Bulletin B68-1. pp. lb-3b.
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Information on ice albedo is required for evaluating
the winter heat budget; developing forcasting techniques
and evaluating ice prevention or removal methods.
Incident and reflected radiation of 8 types of ice
common to the Great Lakes was measured by classical
pyronometers and the output measured by potentiometer.
Albedo varied from 10% for clear ice to 46$ for snow
ice.
37. Bolton, T. E. 1957. Silurian stratigraphy and
paleontology of the Niagara escarpment in Ontario.
Canada Department of Mines and Technical Surveys,
Geological Survey of Canada. Memoir 289. 145 p.
+ plates.
This report describes the result of a detailed study
of sections exposed on Manitoulin Island and along the
Niagara escarpment from Niagara Falls to the Bruce
Peninsula. The various groups, formations and members
into which the Silurian has been divided in different
parts of Ontario are described and correlations suggested
on the basis of observed facies changes and paleontolo-
gical evidence.
38. Brebner, A. and R. J. Kennedy. 1966. Correlation of
waves and shore winds, Lake Ontario. Proceedings
5th Conference Great Lakes Research, Great Lakes
Research Division, Univ. of Michigan, Ann Arbor,
Michigan, pp. 116-123.
Wave characteristics at any geographical location are
a function of the meteorology of the surrounding area.
Mathematical and graphical correlations are drawn
from data concerning the relationships of meteorological
conditions, especially wind direction and velocity and
wave direction and height. It is pointed out that the
correlation only holds true for larger waves due to the
variability of lower intensity winds.
Brodfeld, B. - See: R. W. Gunwaldsen, No. 19**.
Broughton, J. G. - See: D. W. Fisher, No. 172.
39. Broughton, J. G., D. W. Fisher, W. Isachsen and L. V.
Richard. 1962. The geology of New York State.
New York State Museum and Science Service, Map
and Chart Series No. 5. 42 p. + charts.
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Included Is a discussion of the following geologic time
periods: Pleistocene, Precambrain, Paleozoic, Mesozoic
and Cenozoic. Parameters include topography, rock types,
structural geology, physiographic provinces and tertiary
history. Also Included is a discussion of economic
mineral deposits divided according to non-metals, metals
and mineral fuels.
40. Browzin, B. S. 1962. On classification of rivers in
the Great Lakes - St. Lawrence Basin. Proceedings
5th Conference Great Lakes Research, Great Lakes
Research Division, Univ. of Michigan, pp. 86-92.
The relationship of runoff, topography and drainage in
relationship to the flow volume of a river. The flow
volume and its various characteristics and changes are
used as the major classification factor for the Great
Lakes Rivers Including the St. Lawrence River.
41. Browzin, B. S. 1966. Annual runoff in the Great Lakes -
St. Lawrence basin. Proceedings 9th Conference
Great Lakes Research, Great Lakes Research Division,
Univ. of Michigan. Publication 15. pp. 203-220.
The annual runoff of the Great Lakes - St. Lawrence
basin, expressed in terms of unit runoff, increases
from southwest to northeast approximately six times,
which is an unusual characteristic of a river basin.
The responsible factors, precipitation and its seasonable
distribution, as well as mean annual temperature vary
considerably but not gradually from the middle west
portion of the basin to the coast of the Atlantic.
Frequency analysis based on available data at gauging
stations located in various climatic zones of the basin
has shown that the frequency distribution of the annual
runoff is moderate to low as compared to other basins
with similar geographic conditions.
Bruce, J. P. - See: D. V. Anderson, No. 11
42. Bruce, J. P. 1959. Rainfall intensity-frequency
maps for Canada. Department of Transport, Meteoro-
logical Branch, Canada. Circular 3243, Tec. 308.
27 p.
It is not surprising that one of the most common requests
for climatological information received by the Meteoro-
logical Branch is for recurrence frequencies of short
duration rainfalls of high intensities. Engineers make
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frequent use of such data in dealing with drainage
problems. Road culverts, storm sewers, farm pond dams,
airport drainage facilities, roof drainage and flood
control programs on small streams are all designed on
the basis of a flood of a specific average return
period derived from the rainfall intensity for such a
return period. Other applications of such rainfall
frequency figures are in problems of soil erosion,
microwave transmission, air pollution washout, etc.
(Univ. of Toronto, Great Lakes Institute).
43. Bruce, J. P., D. P. Anderson and Q. K. Rodgers. 1961.
Temperature, humidity and wind profiles over the
Great Lakes. Great Lakes Research Division,
Publication No. 7. Univ. of Michigan, pp. 65-70.
This preliminary report on measurement of temperature,
humidity and wind profiles by means of the new meteoro-
logical boom on the research vessel, Porte Dauphine
suggests that considerable effort must yet be put for-
ward to convert the readings into reliable profiles.
A single instrument such as mounted on the bow of the
Porte Dauphine affords a movable, multiple reading
device which can take instantaneous samples of several
parameters without accuracy loss due to time or position
intervals.
44. Bruce, J. P. and G. K. Rodgers. 1962. Water balance
of the Great Lakes system. In: Great Lakes
Basin. American Association Advancement of Science.
Publication No. 71. pp. 41-70.
The water balance of the Great Lakes system depends
on precipitation, evaporation, inflow and outflow
volumes. Computations of evaporation from Lake Ontario
by mass transfer and energy budget methods are presented.
The estimated annual evaporation from Lake Ontario is
2.8 feet.
45. Brunk, I. W. 1964, Hydrology of Lakes Erie and
Ontario. Proceedings 7th Conference on Great
Lakes Research, Great Lakes Research Division,
Univ. of Michigan, pp. 205-216.
A study of the hydrologic characteristics of the Erie
and Ontario basins indicates significant differences.
In the Erie basin only about 1/3 of the precipitation
becomes stream flow - apparently the lowest proportion
for any of the Great Lakes basins. In the Ontario
-34-
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basin the stream flow is equivalent to approximately
1/2 of the precipitation. It appears that factors
other than climate are responsible for these differece
in hydrologic characteristics. There is a large var-
iation in the various river basins which drain into
Erie and Ontario, and also in the months of the year,
in the percentages of the precipitation which flows
into the lakes. The monthly extremes for Lake Erie
range from 75% in March to only 8$ in September. For
Ontario, the figures are 117? in April to 17% in August.
The water area of Lake Erie makes little contribution
to the total water supply of the Great Lakes, because
the average annual evaporation of approximately 34
inches is about the same as the average annual precipi-
tation on the water surface of the lake. The average
monthly evaporation from Lake Erie is largest in Octo-
ber - about 6 1/2 inches. For Lake Ontario, the
apparent average annual evaporation is between 29 and
30 inches.
Brutsaert, W, - See: S. L. Yu, No. 438.
46. Brutsaert, W. and S. L. Yu. 1969. Hydrologic analyses
for Lake Ontario: Stochastic aspects of evapora-
tion. Cornell University Water Resource and
Marine Sciences Center, Ithaca, New York. Technical
Report No. 12. Various pages.
Monthly mean values of evaporation from Lake Ontario
for the period from l8?2 to 1965 Inclusive were genera-
ted by a mass-transfer procedure. Available on-shore
recorded meteorological data were adjusted to obtain
approximate over-lake values with empirically derived
equations. The mass-transfer coefficient was calculated
by using an equation, proposed by Horbeck (1962),
relating the coefficient with water surface area. A
comparison of the generated mass-transfer evaporation
data with water-budget estimates obtained by Morton
(196?) revealed that on the average, the two methods
gave comparable results. (Canada Centre for Inland
Waters).
47. Bubeck, R. C., W, H. Diment, B. L. Deck, A. L. Baldwin
and S. D. Lipton. 1971. Runoff of deiclng salt:
Effect on Irondequoit Bay, Rochester, New York.
Science. 172: 1128-1132.
Salt used for deicing the streets near Rochester, New
York, has increased the chloride concentration in
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Irondequoit Bay at least five-fold during the past two
decades. During the winter of 1969-70, the quantity
and salinity of the dense runoff that accumulated on
the bottom of the bay was sufficient to prevent com-
plete verticle mixing of the bay during the spring.
Comparison with 1939 conditions Indicates that the
period of summer stratification has been prolonged a
month by the density gradient imposed by the salt
runoff.
48. Buehler, E. G. 1966. Geology of Western New York -
guide book. New York State Geological Association,
38th Annual Meeting. State University of New York
at Buffalo. 116 p.
A compilation of many technical articles on the evolu-
tion and geology of specific rock formations found in
Western New York. The major articles presented are:
1. Pre Clinton Rocks in the Niagara Frontier -
D. W. Pisher.
2. Middle Silurian Clinton Relationships of
Western New York and Ontario - W. J. Kilgour.
3. The Lockport Formation in Western New York -
D. H. Zenger.
4. Uuper Silurian Series, Niagara Frontier, New
York - L. V. Rickard.
5. Bois Blanc and Onondaga Formations in Western
New York and Adjacent Ontario - W. A. Oliver, Jr.
6. The Hamilton Group in Western New York - E. J.
Buehler.
7. Upper Devonian Stratigraphy and Paleonlology
of Southwestern New York State (Erie, Chau-
tauqua, Cattaraugus Counties) - I. H. Tesmer.
8. Gonlatite Zonatlon of the New York State
Devonian - M. R. House.
9. Late Pleistocene History of Northwestern New
York - P. C. Calkin.
10. The Economic Geologic Setting of Western New
York - J. S. King.
11. The Gypsum Deposits of the Salina Group of
Western New York - C. V. Clemency.
(Schoellkopf Museum, Niagara Falls, New York).
49. Caley, J. F. 1940. Palaeozoic geology of the Toronto-
Hamilton area, Ontario. Geological Survey of
Canada. Memoir 224. 284 p.
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A documented and detailed map of the western shore of
Lake Ontario between Niagara-on-the-Lake and Bronte,
Ontario showing prominent geological characteristics.
50. Campbell, N. J. and R. K. Lane. 196?. Federal lira-
nological research program on Lake Erie and Lake
Ontario. In: Water for Peace. United States
Government Printing Office. 4: 627-630.
In 19663 the Canadian Department of Energy, Mines and
Resources began an investigation of heat budget, dis-
tribution and storage in Lake Erie and Lake Ontario.
The article discusses data and methods but draws no
conclusions. Future study plans are discussed in this
area.
51. Canada Centre for Inland Waters. 1969a. Lake Ontario
limnological data report No. 1, 1966. Canadian
Oceanographic Data Centre, Burlington, Ontario.
40 p.
This report is one of a series listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Government of Canada agencies.
This report contains water quality data obtained on
two cruises of Lake Ontario. The first cruise (a)
extended from June 1-5, 1966, and consisted of 35
sampling locations siutated on the eastern end of the
lake. The second cruise (b) was made fron June 7-10,
1966, and 39 sampling locations were established over
the entire lake except the extreme west end.
52. Canada Centre for Inland Waters. 1969b. Lake Ontario
limnological report No. 2, 1966. Canadian
Oceanographic Data Centre, Burlington, Ontario.
This report is one of a series listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Government of Canada agencies.
This report contains data on water quality obtained
on a single cruise extending from June 15-19, 1966,
on the Eastern end of Lake Ontario.
53. Canada Centre for Inland Waters. 1969c. Lake Ontario
limnological data report No. 3, 1966. Canadian
Oceanographic Data Centre, Burlington, Ontario.
88 p.
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This report is one of a series listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Government of Canada agencies.
This report contains water quality data obtained on a
single cruise extending from June 21-25, 1966, and
covering the entire lake.
5h. Canada Centre for Inland Waters. 196'9d. Lake Ontario
llmnologlcal data report No. 4, 1966. Canadian
Oceanographic Data Centre, Burlington, Ontario.
113 p.
This report is one of a series listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Canadian Government agencies.
This report contains x^ater quality data obtained on a
single cruise extending from June 26-30, 1966, and
covering the area along the American shoreline with
the exception of the far western end of the lake.
55. Canada Centre for Inland Waters. 1969e. Lake Ontario
limnologlcal data report No. 5, 1966. Canadian
Oceanographic Data Centre, Burlington, Ontario.
125 p.
This report is one of a series listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Canadian Government agencies.
Data of Lake Ontario water samples collected on a
single, lakewide cruise extending from July 4-10,
1966, are tabulated in this report.
56. Canada Centre for Inland Waters. 1969f. Lake Ontario
llmnological data report No. 6, 1966. Canadian
Oceanographic Data Centre, Burlington, Ontario.
116 p.
This report is one of a series listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Canadian Government agencies.
This report contains water quality data obtained on
two cruises of Lake Ontario. The first cruise (a)
extended from July 12-15, 1966, and consisted of 75
sampling locations situated over the entire lake except
for the far eastern end. The second cruise (b) was
made from July 19-24, 1966, and 88 sampling stations
were established over the entire lake.
-38-
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57. Canada Centre for Inland Waters. 1969g. Lake Ontario
limnological data report No. 7, 1966, Canadian
Oceanographic Data Centre, Burlington, Ontario.
113 P.
This report is one of a series listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Canadian Government agencies.
This report contains water quality data obtained on two
cruises of Lake Ontario. The first cruise (a) extended
from July 26-29, 1966, and consisted of 62 sampling
locations centered around two points on either side of
mid lake. The second cruise (b) was made from August
2-7, 1966, and 79 sampling stations were established
over the entire lake.
58. Canada Centre for Inland Waters. 1969h. Lake Ontario
limnological data report No. 9, 1966. Canadian
Oceanographic Data Centre, Burlington, Ontario.
119 p.
This report is one of a series listing chemical,
bacteriological and physical data for Lake Ontario
observed by Canadian Government agencies.
This report contains extensive water quality data
obtained on two cruises of Lake Ontario. The first
cruise (a) occured in the period of August 15-19, 1966,
and Involved 69 samplings located lakewide. The second
cruise (b) extended from August 29 - September 2, 1966,
and consisted of 47 sampling locations situated around
the Lake.
59- Canada Centre for Inland Waters. 19691. Lake Ontario
limnological data report No 10, 1966. Canadian
Oceanographic Data Centre, Burlington, Ontario.
80 p.
This report is one of a series listing chemical,
bacteriological and physical data from Lake Ontario
observed by Canadian Government agencies. «
This report contains water quality data obtained from
two cruises of Lake Ontario. The first cruise (a)
took place between September 6-11, 1966, and covered
the area around Toronto, midlake, and an extensive
section of the eastern end of the lake. The second (b)
cruise extended from September 12-16, 1966, and was
lakewide.
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60. Canada Centre for Inland Waters. 1969J . Lake Ontario
limnological data report No. 11, 1966. Canadian
Oceanographlc Data Centre, Burlington, Ontario.
109 p.
This report is one of a series listing chemical,
bacteriological and physical data for xvaters of Lake
Ontario, observed by Canadian Government agencies.
This report contains data of water samples collected
on a single cruise extending from September 20-24, 1966,
around the mouths of Niagara, Oswego, Genesee and St.
Lawrence Rivers.
61. Canada Centre for Inland Waters. 1969k. Lake Ontario
limnological data report No. 12, 1966. Canadian
Oceanographic Data Centre, Burlington, Ontario.
73 P.
This report is one of a series listing data from chemical,
bacteriological and physical studies of waters of Lake
Ontario, observed by Canadian Government agencies.
This report contains water quality data obtained on
two cruises of Lake Ontario. The first (a) extended
from September 26-29, 1966, and was lakewide. The
second (b) extended from October 1-3, 1966, and
covered the eastern end of the lake.
62. Canada Centre for Inland Waters. 1970a. Lake Ontario
limnological data report No. 1, 1967. Canadian
Oceanographic Data Centre, Burlington, Ontario.
212 p.
This report is one of a series listing chemical,
bacteriological and physical data from water samples
from Lake Ontario, observed by Canadian Government
agencies.
This report contains data of water samples collected
on three lakewide cruises. The first cruise (a) con-
sisted of 73 sampling stations, the second (b) of 73
and the third (c) of 62.
63. Canada Centre for Inland Waters. 1970b. Lake Ontario
limnological data report No. 2, 1967. Canadian
Oceanographic Data Centre, Burlington, Ontario.
232 p.
-------
This report is one of a series listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Canadian Government agencies.
This report contains data of water samples collected
on two lakewide cruises. The first (a) extended from
July 25-30, 1967, and the second (b) from August 5-10,
1967.
64. Canada Centre for Inland Waters. 1970c. Lake Ontario
limnological data report No. 3, 1967. Canadian
Oceanographic Data Centre, Burlington, Ontario.
179 P.
This report is one of a series listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Canadian Government agencies.
This report contains data of water samples collected
on three lakewide cruises. The first cruise (a)
extended August 21-25, 1967, the second (b) from
September 5-9, 1967 and the third (c) from September
16-21, 1967.
65. Canada Centre for Inland Waters. 1970d. Lake Ontario
limnological data report No. 4, 1967. Canadian
Oceanographic Data Centre, Burlington, Ontario.
203 p.
This report is one of several listing chemical,
bacteriological and physical data for waters of Lake
Ontario, observed by Canadian Government agencies.
This report contains data of water samples collected
on three lakewide cruises. The first cruise (a)
extended from October 1-6, 1967, the second (b) from
October 17-21, 1967 and the third (c) from October
28 - November 2, 1967.
66. Canada Centre for Inland Waters. 1970e. Lake Ontario
limnological data report No. 1, 1968. Canadian
Oceanographic Data Centre, Burlington, Ontario.
85 p.
This report is one of several listing chemical,
bacteriological and physical data for Lake Ontario
waters by Canadian Government agencies.
-------
This report contains data of water samples collected
on three lakewide cruises. The first cruise (a) extended
from April 30 - May 3, 1968, the second (b) from May
27-30, 1968 and the third (c) from July 2-6, 1968.
67. Canada Centre for Inland Waters. 1970f. Lake Ontario
limnological data report No. 2, 1968. Canadian
Oceanographic Data Centre, Burlington, Ontario.
66 p.
This report is one of several listing chemical,
bacteriological and physical data for Lake Ontario
waters by Canadian Government agencies.
This report contains data of water samples collected
on three lakewide cruises. The first cruise (a) extended
from July 23-28, 1968, the second (b) from August 19-22,
1968 and the last (c) from September 8-13, 1968.
68. Canada Centre for Inland Waters. 1970g. Lake Ontario
limnological data report No. 3, 1968. Canadian
Oceanographic Data Centre, Burlington, Ontario.
100 p.
This report is one of several listing chemical,
bacteriological and physical data for Lake Ontario
waters observed by Canadian Government agencies.
This report contains data of water samples collected
on three lakewide cruises. The first cruise (a) extended
from October 5-9, 1968, the second (b) from October
27-31, 1968 and the last (c) from November 17-22, 1968.
69. Canadian Department of Energy, Mines and Resources.
1964. Great Lakes water levels. Inland Waters
Branch, Great Lakes Division, Ottawa. 14 p.
The major source of water in the Great Lakes is from
precipitation and stream runoff. Water elevation is
relatively stable with slight yearly and cyclical
seasonal lake level variation. In 1958, as part of
the St. Lawrence seaway project, dams were built at
the outflow of Lake Ontario which have since that time
regulated and stabilized lake level.
Three interbasin diversions operate in the Great Lakes,
the Long Lac and Ogahi diversions that channel water
from Hudson Bay tributaries into Lake Superior and the
Chicago diversion that takes water from Lake Michigan
and puts it into the Mississippi basin.
-------
Water level control by diversion and darning outflows
has, therefore, relatively stabalized the lake levels
allowing for partial human control. (Canada Centre
for Inland Waters).
70. Canadian Department of Energy, Mines and Resources.
1966. Ontario surface water data. Water Survey
of Canada, Ottawa. 277 p.
Data on tributaries to Lake Ontario. Parameters
discussed are: location, drainage area, apparatus,
period of record, discharge. The volume parameters
are given daily and monthly.
71. Canadian Department of Energy, Mines and Resources.
1967a. Ontario surface water data. Water Survey
of Canada, Ottawa. 303 p.
Data on tributaries to Lake Ontario. Parameters
discussed are: location, drainage area, gauge appara-
tus, period of record, discharge/day/month.
72. Canadian Department of Energy, Mines and Resources.
1967b. Water levels, 1966. Great Lakes St.
Lawrence River System. Inland Waters Branch,
Ottawa. Vol. 1. 3^5 p.
The water levels compiled in this book were tabulated
from continuous records obtained throughout the year.
Data include daily and monthly means, high and low
water levels and high and low tide levels.
73- Canadian Department of Energy, Mines and Resources.
1968. Water levels, 1967. Great Lakes St.
Lawrence River System. Inland Waters Branch,
Ottawa. Vol. 1. 187 p.
The water levels compiled in this book were tabulated
from continuous records obtained throughout the year.
Data include daily and monthly means, high and low
water levels and high and low tide levels.
71*. Canadian Department of Fisheries and Forestry. 1969.
Water levels, 1968. Great Lakes St. Lawrence
River System (non-tidal). Marine Science Branch,
Ottawa. Vol. 1. 191 p.
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The water levels compiled in this book were tabulated
from continuous records obtained throughout the year.
Data include daily and monthly means, high and low
water levels and high and low tide levels.
75. Canadian Department of Fisheries and Forestry. 1970.
Water levels, 1969. Great Lakes St. Lawrence
River System (non-tidal). Marine Science Branch,
Ottawa. Vol. 1. 195 p.
The water levels compiled in this book were tabulated
from continuous records obtained throughout the year.
Data include daily and monthly means, high and low
water levels and high and low tide levels.
76. Canadian Department of Fisheries and Forestry. 1971.
Water levels, 1970. Great Lakes St. Latirrence
River System (non-tidal). Marine Science Branch,
Ottawa. Vol. 1. 199 P.
The water levels compiled in this book were tabulated
from continuous records obtained throughout the year.
Data include daily and monthly means, high and low
water levels and high and low tide levels.
77. Canadian Department of Mines and Technical Surveys.
1963. Water levels, 1962. Great Lakes St.
Lawrence River System, Atlantic Coast and Artie
Coast. Marine Science Branch, Ottawa. 95 p.
The water levels compiled in this book were tabulated
from continuous records obtained throughout the year.
Data include daily and monthly means, high and low
water levels and high and low tide levels.
78. Canadian Department of Mines and Technical Surveys.
1964. Water levels, 1963. Great Lakes St.
Lawrence River System, Atlantic Coast, Hudson
Bay and Artie Waters and Pacific Coast. Marine
Science Branch, Ottawa. 170 p.
The water levels compiled in this book were tabulated
from continuous records obtained throughout the year.
Data include daily and monthly means, high and low
water levels and high and low tide levels.
-44-
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79. Canadian Department of Mines and Technical Surveys.
1965. Water levels, 1964. Great Lakes St.
Lawrence River System, Atlantic Coast, Hudson
Bay and Arctic Waters, Pacific Coast. Marine
Science Branch, Ottawa. 270 p.
The water levels compiled in this book were tabulated
from continuous records obtained throughout the year.
Data include daily and monthly means, high and low
water levels and high and low tide levels.
80. Canadian Department of Mines and Technical Surveys.
1966. Water levels, 1965. Great Lakes St.
Lawrence River System (non-tidal). Marine
Science Branch, Ottawa. Vol. 1. 166 p.
The water levels compiled in this book were tabulated
from continuous records obtained throughout the year.
Data include daily and monthly means, high and low
water levels and high and low tide levels.
81. Canadian Department of Northern Affairs and National
Resources. I960. St. Lawrence and southern
Hudson Bay drainage - 1956-57. Water Resources
Paper No. 119, Ottawa. 544 p.
The report contains discharge and runoff data for the
following rivers in the Ontario Basin.
Niagara River Humber River and Branches
Welland River Dan River
Twenty Mile Creek Highland Creek
Oakville Creek Rouge River
Credit River Duffin Creek
Etobicoke River Ganarasha River
Trent River Nepanee River
Depot Creek Mocra River with Skootamatta
River and Black River
82. Canadian Department of Northern Affairs and National
Resources. 1962a. St. Lawrence and southern
Hudson Bay drainage - 1957-58. Water Resources
Paper No. 126, Ottawa. 326 p.
The report contains discharge and runoff data for the
following rivers in the Ontario Basin.
-------
Niagara River Humber River and Branches
Welland River Dan River
Twenty Mile Creek Highland Creek
Oakville Creek Rouge River
Credit River Duffin Creek
Etobicoke River Ganarasha River
Trent River Nepanee River
Depot Creek Mocra River with Skootamatta
River and Black River
83. Canadian Department of Northern Affairs and National
Resources. 1962b. St. Lawrence and southern
Hudson Bay drainage - 1958-59. Water Resources
Paper No. 129, Ottawa. 328 p.
The report contains discharge and runoff data for the
following rivers in the Ontario Basin.
Niagara River Humber River and Branches
Welland River Dan River
Twenty Mile Creek Highland Creek
Oakville Creek Rouge River
Credit River Duffin Creek
Etobicoke River Ganarasha River
Trent River Nepanee River
Depot Creek Mocra River with Skootamatta
River and Black River
84. Canadian Department of Northern Affairs and National
Resources. 1963. St. Lawrence and southern
Hudson Bay drainage - 1959-60. Water Resources
Paper No. 133 3 Ottawa. 352 p.
The report contains discharge and runoff data for
the following rivers in the Ontario Basin.
Niagara River Humber River and Branches
Welland River Dan River
Twenty Mile Creek Highland Creek
Oakville Creek Rouge River
Credit River Duffin Creek
Etobicoke River Ganarasha River
Trent River Napanee River
Depot Creek Mocra River with Skootamatta
River and Black River
-------
85. Canadian Department of Northern .Affairs and national
Resources. 1961!. St. Lawrence and southern
Hudson Bay drainage •- 19tQ-Cl. V/ater Resources
Paper No. 1373 Ottawa. 376 p.
The report contains discharge and runoff data for the
following rivers in the Ontario Basin.
Niagara River " Kuro&er River aid Branches
Welland River Dan River
Twenty Mile Creek Highland Creek
Oakvlile Creek Rouge River
Credit River Duffin Creek
Etobicoke River Ganarasha River
Trent River Nepanee River
Depot Creek Mocra River with Skootamatta
River and Black River
86. Canadian Department Northern Affairs and National
Resources. 1965. St. Lawrence and southern
Hudson Bay drainage - 1962-63. Water Resources
Paper No. 143, Ottawa. 352 p.
The report contains discharge and runoff data for
the following rivers in the Ontario Basin.
Niagara River Humber River and Branches
Welland River Dan River
Twenty Mile Creek Highland Creek
Qakvllle Creek Rouge River
Credit River Duffin Creek
Etobicoke River Ganarasha River
Trent River Napanee River
Depot Creek Mocra River with Skootamatta
River and Black River
87, Canadian Department of Northern Affairs and National
Resources, 1966. St. Lawrence and southern
Hudson Bay drainage water year 1963-64. Water
Resources Paper No, 1^7, Ottawa. 368 p.
The report contains discharge and runoff data for
the following rivers In the Ontario Basin.
Niagara River Humber River and Branches
Welland River Dan River
Twenty Mile Creek Highland Creek
Oakvlile Creek Rouge River
-------
.Credit River Duffin Creek
Etobicoke River Ganarasha River
Trent River Nepanee River
Depot Creek Mocar River with Skootamatta
River and Black River
Canadian Department of Transport. 1959a. Break-up
and freeze-up dates of rivers and lakes in Canada.
Meteorological Branch Circular 3156, Ottawa, Ice
2. 91 p.
The time at which ice in rivers and lakes breaks up
in the spring, and reforms again in the fall, is of
great importance to many public and private agencies.
Ice is of particular concern to ship operators, fish-
ermen, aircraft operators, logging Interests and
power companies.
The dates of break-up and freeze-up of rivers and lakes
in the immediate vicinity of meteorological stations
have been obtained for past years for as long a period
as possible. The results from the survey are listed in
this publication. Data on break-up and freeze-up has
been obtained for 8? rivers, and 113 lakes, bays and
harbours. The length of the individual records varied
from one year, to 128 years for the Miramichi River at
Chatham, N. B., and 130 years for the St. John River
at Frederlcton, N. B.
The information on break-up indicated the data on which
the ice first moved or showed signs of breaking, and
also the date on which the water was entirely clear of
ice. Similarly for freeze-up, the date on which ice
first formed and the date on which the body of water was
completely frozen over was listed. Data was obtained
from a wide variety of sources including station meteoro-
logical records, newspaper files, power companies, public
utility companies, harbour commissions, transportation
companies, church missions, ROMP., other governmental
agencies and many private companies and individuals.
Since the original survey, a regular program for the
reporting of dates of break-up and freeze-up at
selected meteorological stations has been instituted.
Additional data obtained as a result of this program
will be published when available.
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The following tables list all the data concerning
break-up and freeze-up in Canada, which is presently
available to the Meteorological Branch. Where the
length of record is ten years or more, mean dates are
given, and extreme dates are underlined. (Univ. of
Toronto, Great Lakes Institute).
89. Canadian Department of Transport. 1959b. Maximum winter
ice thinkness in rivers and lakes in Canada.
Meteorological Branch Circular 3195, Ottawa. Ice-4.
19 P.
As the result of a survey of Canadian Meteorological
stations in 1956 and 1957, and a continued reporting
program by stations since that time, the dates of break-
up and freeze-up of 195 rivers and lakes in Canada were
obtained for varying number of years. The results of
this survey were published in Circular 3156 ICE-2 30 Jan.
59. In this report, meteorological stations were also
requested to report the maximum winter ice thickness
vrtiich attained in the body of water concerned, if this
information could be obtained.
The ice thickness data has been collected for 78 lakes
and 42 rivers at 125 locations In Canada, and is listed
in this circular. In most instances, data are available
for 1957 and 1958 only, but six stations have provided
data for periods exceeding 15 years. (Univ. of Toronto,
Great Lakes Institute).
90. Canadian Department of Transport. 1964. Aerial ice
observing and reconnaissance. Meteorological
Branch, Great Lakes Circular 3987, Ottawa. Ice-13.
25 P.
This is the twenty-second report in the series concerning
ice conditions observed by aerial ice reconnaissance con-
ducted by the Basic Weather Division, Meteorological
Branch, Department of Transport.
This report described observed ice conditions, with
regard to ice coverage, age, topography, puddling, snow
cover and water features over the area of Lake Superior,
the North Channel, Georgian Bay, Lake Huron, Lake Erie,
Lake Ontario and adjacent waterways, during the period
December, 1962 to April, 1963- (Univ. of Toronto, Great
Lakes Institute).
-49-
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91. Canadian National Committee. 196?. Canadian research
basin. Ottawa, Ontario. Unnumbered.
Basic data on a few smaller tributary basins flowing
into Lake Ontario. Location, elevation water flow,
development and experimentation parameters are discussed.
(Canada Centre for Inland Waters).
92. Cartier, R. H. 1968. Pollution, oceanography and
limnology in the Great Lakes. l?th International
Congress of Limnology, Jerusalem, Israel, pp. 60-68.
A listing of research parameters to be investigated by
various research organizations during the International
Field Year-Great Lakes. They include:
1. Lake Meteorology - evaporation, aerial distribution
of precipitation, air-water interface, definition
of lake wind-field, lake influence on atmosphere
and climate.
2. Reassessment of water budget terms - inflow, outflow,
precipitation, evaporation, ground water contribu-
tion, soil moisture levels, diversing and
consumptive use.
3. Energy Balance - energy exchange, transport and
thermal characteristics.
4. Water Movement - currents, seiches, waves,
diffusion, shore and bottom processes.
5. Interdisciplinary Problems - water levels.
93. Chalmers, R. 1905a. Changes in the levels of the
Great Lakes. Geological Survey of Canada. Annual
Report (New Series). 14: 169A.
It is evident that Huron, Erie and Lake Ontario stood
at higher levels at the close of the Pleistocine period
than they do at present time. In the subsistence of
the waters that followed, the various lakes reached a
level considerably lower than present levels. This low
level stage probably occurred in the Recent Period, that
is, since the latest of the Pleistocene beds were laid
down. In the Lake Ontario Basin, the Humber, Don and the
Cataraqui at Kingston have the lower parts of their
courses flooded from the lakes. The lake must have been
25-30 ft. lower at the time to allow for the channel
erosion.
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9*J. Chalmers, R. 1905b. Sand dunes and spits. Geological
Survey of Canada. Annual Report (New Series). 14:
170A.
In the Lake Ontario Basin, the sand driftage has been
from east to west. Toronto Island and Burlington Beach
may have been formed by this movement. These beach
formations exemplify the conditions which prevailed in
the interglacial period in this region when land and
fresh water shells were buried together in the clay and
sand beds of that time.
Chandler, D. C. - See: A. M. Beeton, No. 29.
95. Chandler, D. C. 1964. The St. Lawrence Great Lakes.
Great Lakes Verh. Internat. Verin. Limnol. 15:
59-75.
General geographical, morphometrlc and limnological
data pertaining to the Great Lakes. Included is a
listing of contemporary research and funding organi-
zations and programs.
96. Chapman, L. J. and D. P. Putnam. 1937. The soils of
south central Ontario. Sci. Agr. 18(4): 161-197.
The southern part of Central Ontario has an interesting
and, in some respects, unusual set of soils. Because
of the complex geological history of the parent
materials, the types are many and varied; hence a com-
plete classification of all the members and an accurate
mapping of the same will come only with a detailed soil
survey. In the meantime, it is useful to have a
general description embodying those physical factors,
such as topography, drainage, depth and stonlness, which
limit theuse of land, as well as those factors of
natural fertility which govern soil treatments. Finally
by taking into consideration the morphological features
of the soil profiles, and by grouping those types which
show similarity in the chief characteristics, it is
possible to classify thirteen land types which constitute
fairly well define units in the study of agricultural
adaptation. It is, therefore, to be hoped that this
account of the soils of south-central Ontario will serve
the purposes of geographers and ecologists, and until
more detailed soil surveys are made, will constitute a
guide to soil treatments, as well as a basis upon which
to plan actual tests with fertilizers and different
varieties of crop plants. (Univ. of Toronto, Zoology
Library).
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97. Chapman, L. J. and D. P. Putnam. 1939. The physio-
graphy of eastern Ontario. Sci. Agr. 20(7): 424-
441.
Eastern Ontario comprises that part of the St. Lattfrence
lowland lying within the Province east of Kingston. It
is largely underlain by sedimentary rock of the Ordovician
system which have departed but little from their original
horizontal attitude, but it also Includes the more low-
lying border areas of the Laruential Shield, some of
which were undoubtedly covered, before glaciation, by
sedimentary rock. Subsequent to glaciation, it was
drowned by the sea and so its surface in part Is now
covered by unconsolldated deposits, but there are large
areas of very shallow drift and rock outcrop.
In some instances, the same type of topography and
surface deposit are present in continuous areas of
several hundred square miles, while other sections are
much less uniform and consist of a patchwork of several
types. We have not attempted to name and describe
individually each of the smaller units but they have
been classified and mapped under seven categories, the
chief characteristics of which have been summarized in
Table 1.
As was the case in Central Ontario (13), the present
study was undertaken to provide a basis for the classi-
fication of surface geological materials in the course
of reconnaissance soil survey. It has been shown in
South-Central Ontario (1) and in South-Western Ontario,
as well, (12) that a strong correlation exists between
the geological materials and the chemical properties
of the soils developed from them. This is in accordance
with the well known pedological principal that young
soils exhibit more of the characteristics of the parent
materials than do more mature soils in which the zonal
or climatically determined features are predonimant.
98. Chapman, L. J. and D. F. Putnam. 1942. The soils of
eastern Ontario. Scl. Agr. 22(10): 608-636.
The soils of Eastern Ontario are younger than those of
Central and Southwestern Ontario, hence leaching has
proceeded for a shorter length of time. However, this
is counter-balanced by a colder climate which results
In more severe leaching here, especially up the Ottawa
Valley where coniferous forests are found.
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As a result of level topography, drainage is poor in
about half of the area, constituting a major problem
for the farmers of the region. On higher sites, the
most obnoxious characteristic is stoniness. Some of
the best land was originally either poorly drained
or stony. The poor land is made up of the shallow,
sandy, wet and stony, or excessively stone soil and
bog. On this basis, there is more poor land than
good, the aereal ratio being about 60 to 40.
The chemical nature of the soils were studied through
a collection of 464 samples taken from hay and pasture
fields. After testing these samples, it is possible
to point out the soils with the most, least and an
intermediate amount of lime, phosphate or potash.
Furthermore, an attempt was made to divide the area
into zones with similar fertilizer and lime require-
ments. The need of experimental work in certain cases
is also indicated and those soils considered unworthy
of expensive treatment under present economic condi-
tions are also mapped.
An added item of description is the table of numerical
ratings for each type of land as to its ability to
produce several staple crops. It is intended that
more specific studies will be made on the adaptation
of crops; that is, one of the main reasons for making
this survey of the soils. (Univ. of Toronto, Zoology
Library).
99. Chapman, L. J. and D. P. Putnam. 1943- The moraines
of southern Ontario. Transactions Royal Society
of Canada. Section 4: 33-41.
The moraines north of Lake Ontario were formed by the
actions of two ice masses, one in the Lake Ontario
Basin, the other advancing from the north. The action
and Interaction produced several prominent moraines in
the area. Discussed are the Oak Ridges and Scaroborough
Moraines.
100. Chawla, V. K. and J. W. Traversy. 1968. Methods of
analysis on Great Lakes waters. Proceedings llth
Conference Great Lakes Research, pp. 524-530.
Methods of the analytical section, Water Quality Division,
were used to analyze Great Lakes waters aboard ship and
on the shore based laboratory, Burlington, Ontario,
both Lake Erie and Lake Ontario waters were analyzed.
-53"
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At Lake Ontario, three stations were established where
samples were taken at descending depths-two samples/
depth and \^ere analyzed for specific conductance. The
results are in a table.
101. Chermack, E. E. 1970. Study of thermal effluents in
southeastern Lake Ontario as monitored by an air-
borne infrared thermometer. Proceedings 13th
Conferencej Great Lakes Researc. pp. 904-913-
Commensing in July, 1969, and continuing into the 1969-70
winter, twice weekly measurement of lake surface tempera-
tures off che southeastern shore of Lake Ontario have been
made using a Barnes PRT-5 radiation thermometer mounted on
a small aircraft. The object of this research was to
obtain data on the present effluents into the lake power
plants, and to obtain background information on the un-
disturbed lake prior to introduction of new effluents.
Over one half years data has been analyzed. Maps of
the Oswego River and two new power plant effluents are
presented and discussed.
Clark, J. R. - See: P. P. Karrow, No. 228.
102. Clark, L. J. 1891. Currents in Lake Ontario. Trans-
actions Canadian Institute. 3: 275-280.
A general discussion of Lake currents (surface and
internal) alonf? with the factors responsible for the
generation of such currents. A float was used to
tabulate current velocity and direction. Instances
are presented supporting the theory of strong under-
currents in the lake.
103. Clark, L. J. 1892. Currents in Lake Ontario. Trans-
actions Canadian Institute. 2: 154-157.
Currents in Lake Ontario do not follow a regular, con-
stant, well defined pattern. The currents are a result
of varying winds, precipitation and atmospheric pressure
which vary greatly from month to month and year to year.
The study of the currents in the Rochester area of U. S.
and Scarborough area of Canada are used. The author
discusses his theory of undercurrents or undertow
currents and relates some shipping phenomenon to the
existence of these.
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104. Claypole, E. W. I88la. Origin of Lakes Erie and Ontario,
Canadian Naturalist. 9- 213-227.
The glacial theory on the origin of the Great Lakes
basin rests on insufficient evidence. The glaciers
could not have eroded so much material., the eroded
material is not found where it should be found if the
theory was true, and there could have been no local
glaciers had the Lake beds not previously existed to
hold them.
Therefore, the river theory should be considered due
to less explanitory difficulty. Lakeo Huron, Erie and
Ontario were formed by widening of areas in a large
pre-glacial river.
105. Claypole, E. W. l88lb. Evidence from the drift of
Ohio, Indiana and Illinois, in support of the
preglacial origin of the basins of Lakes Erie and
Ontario. Proceedings of the American Association
for the Advancement of Science, 30; ]47-159•
The glacial theory is not sufficient to explain the
Great Lakes Basin formation. The glaciers could not
have done the necessary erosion, the deposits are not
in the right position or volume to have been done by
the glacier, and there could have been no glacial
action in the area, had the beds not already existed.
The basins, therefore, are thought to be the result
of an ancient river with the bottling up phenomenon
produced by the glaciers.
106. Claypole, E. W. 1886. The old gorge at Niagara,
Science. 8: 236.
The author hypothesises that a limestone ridge or
block in the old St. Davids Gorge is an indication
that the Niagara River did not flow through the Gorge
as has been believed but the present; s'St. Davids Gorge"
which is now almost entirely filled in by glacial
deposits was formed by a second river flowing into the
Niagara, joining it at the whirlpool section of our
present Niagara River.
107. Coakley, J. P. 1970. Natural and artificial sediment
tracer experiments in Lake Ontario. Proceedings
13th Conference Great Lakes Research, pp. 198-208.
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Thin sand bodies of intermediate surface area overlying
bedrock and glacial deposits occur at intervals in the
nearshore zone of western Lake Ontario between Burling-
ton and Toronto. Natural tracers, i.e. textural and
mineralogical characteristics of the sediments, and
artificially fluorescent sand were used to study trans-
port direction and sediment provenance in this area.
The minerals in the sand bodies were characterized by
angularity and a high proportion of non-resistent min-
erals . Statistical tests on the samples indicated that
the minerology of the sand bodies did not vary signifi-
cantly from sand body to sand body. The combination of
these features suggests derivation from local sources
rather than one external to the area. The textural data
do not contradict this conclusion, but due to the
significant effect of varying water depth over the sand
bodies, more careful sampling is needed to evaluate
their use as sediment transport indicators. This study
indicated that sediment transport direction is related
primarily to the orientation of the shoreline with
respect to easterly winds.
108. Coch, 1. K. 1961. Textural and minerological variations
in some Lake Ontario beach sands. M. S. Thesis,
Univ. of Rochester. 262 p.
1. .* ;ach sands of Lake Ontario are largely derived
* s'n the glacial deposits exposed along the shore.
While a part of the light fraction is derived from
the sedimentary rocks exposed along the shore, the
rest of the light fraction and most (95 percent) of
the heavy mineral fraction is derived from the
igneous and metamorphlc rocks of the Adirondacks and
Greenville Province.
2. The mineralogy of the beach sands is very uniform
along the interval studied, with variations between
samples being due to changes in texture.
3- Glacial deposits on the convex areas are being
actively eroded. The finer fraction of these
deposits is transported east and deposited in
adjacent concave areas.
4. Areas of active wave erosion are characterized by
coarser material on the beaches and a positive
slewness. The reverse is true for sheltered areas.
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5. The higher percentages of hypersthene in the beach
sands west of Sodus Bay suggests that the tills to
the west of Sodus Bay were derived from an area
richer in hypersthene, than those to the east of
Sodus Bay.
6. Beach sediments which have a phi mean less than
1.70 are more poorly sorted than those sediments
which have a phi maan greater than 1.70.
7. Beach sands that are well sorted have higher
kurtosis values than those that are poorly sorted.
8. Better sorted sediments have a higher percentage of
heavy minerals than poorly sorted sediments.
9. Sediments which have a phi mean between 1.5 and
2.5 have the highest percentage of heavy minerals.
109. Coleman, A. P. 1913. III. Geology of the Toronto
region. In: Paull, J. H. (Ed.). The Natural
History of the Toronto region. Canadian Institute,
Toronto, p. 51-81.
Contains a study of the geology of the Toronto region.
Within one hundred miles of Toronto the following geo-
logical formations are displayed:
Recent - shore cliffs and wave-built bars
Pleistocene - glacial, interglacial and post-
glacial beds
Palaeozoic - (1) Devonian - onondaga and Hamilton
beds.
(2) Silurian - cataract, medina, clln-
ton, Niagara and Guelph beds,
(3) Ordovician - Trenton limestone,
Utica and Collingwood shale,
Lorraine shale and Queenston
shale.
Archaean - granites, gneisses, greenstones and
greenschlsts.
Included in the section on glacial lakes is a history
of Niagara Palls. It tells of the formation of the
Falls beginning with the outflow of the Algonquin
waters through the Erie valley and northward over the
Niagara escarpment into the basin of Lake Iroquois.
The gorge is discussed along with the receding of the
Palls.
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Also included is a discussion of the soils and their
formation of the Toronto region. (Toronto-Royal
Ontario Museum).
110. Coleman, A. P. 1922. Glacial and post glacial lakes
in Ontario. Ontario Fisheries Research Laboratory
Publication, No. 10. Univ. of Toronto Studies.
76 p.
The glacial formation of several Ontario lakes through-
out several geological periods is discussed. The
article follows evolutionary geological transformations
during the formation of the Great Lakes from preglacial
times to the present. The preglacial Laurentian River
and its tributaries followed the general flow pattern
of the Great Lakes of today. The outlet in the Ontario
basin was periodically blocked and freed during at least
5 glacial periods. The outlet rose gradually producing
a deeper and larger lake. The outlet since the last
glacial age has dropped approximately 25 feet lowering
the lake level. Many other lakes formed by the glaciers
are discussed.
Ill, Corps of Engineers. Undated. Study of the Lake Erie-
Lake Ontario Canal. U. S. Army Corps of Engineers,
Buffalo District. 5 p.
The building of new Lake Erie-Lake Ontario Canal would
require: straightening, widening and deepening, the
Black Rock Channel; raising or rebuilding bridges that
span the Niagara River between Lake Erie and Tonawanda
Harbor; a thorough review of routes that appear to be
most feasible and economical between North Tonawanda
and Lake Ontario; construction of railxvay and highway
bridges over the selected route of the New Canal; and
the nature and suitability of subsurface material on
which the locks and structures will be built.
Shipping parameters should be investigated and an
extensive cost-benefit study should be undertaken.
112. Corps of Engineers. 1951. Niagara River redevelopment.
U. S. Army Corps of Engineers, Buffalo District.
15 p. and several plates.
Results of seismological testing and stress studies
indicates several stress points in the bedrock of
western New York. Examples of rock movements on
"squeezes" are given along the Erie Canal and Niagara
River. The movement appears to be primarily in the
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dolomites of the area with a general east-west movement.
Core must be taken In tunnel or canal construction to
allot* for some expansion or contraction.
113. Corps of Engineers. 1955. Pair Haven Beach State Park,
New York, beach erosion control study. 84th Congress
1st Session, House Document No. 134, U. S. Government
Printing Office, Washington, D. C. 40 p.
Pair Haven Beach State Park comprises about 1 1/2 miles
of shore on the southern shore near the east end of Lake
Ontario. It is located in the town of Sterling, in
Cayuga County, about 15 miles southwest of Os;vego Harbor.
The purpose of this overall study is to develop the most
suitable plans for the protection of the shores of three
established State parks known as Selkirk Shores State
Park, Pair Haven Beach State Park and Hamlin Beach State
Park, with a view to preventing further erosion of the
shores within these areas and to determine the extent
of Federal participation in the cost of a. project for
beach erosion control. The plans are to include specific
areas within each park by the restoration or creation of
beaches. The present report concerns Pair Haven Beach
State Park only.
11s, Corps of Engineers. 1955. Hamlin Beach State Park,
New York, beach erosion control study. 84th Congress
1st Session, House Document No. 138, U. S. Government
Printing Office, Washington, D. C. 34 p.
Hamlin Beach State Park comprises about 2 1/4 miles of
shore in the central part of the southern shore of Lake
Ontario. It is located in the town of Hamlin in Monroe
County, about 20 miles west of Rochester.
The purpose of this overall study is to develop the most
suitable plans for the protection of the shores of thre«
established State parks known as Selkirk Shores State
Park, Pair Haven Beach State Park and Hamlin Beach State
Park, with a view to preventing further erosion of the
shores within these areas and to determine the extent of
Federal participation in the cost of a project for beach
erosion control. The plans are to Include specific area,,
within each park by the restoration or creation of
beaches. The present report concerns Hamlin Beach State
Park only.
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115. Corps of Engineers. I960. Great Lakes harbors study -
Interim report on Rochester Harbor, New York. 86th
Congress, 2nd Session, House Document No. 409, U. S.
Government Printing Office, Washington, D. C. l\6 p.
Rochester Harbor is located at the mouth of the Genesee
River on the south shore of Lake Ontario. This interim
report considers channel deepening and widening and
dredging an upstream turning basin, all in the Interests
of deep-draft bulk cargo traffic.
116. Corps of Engineers. 1961. Great Lakes harbors study -
Interim report on Great Sodus Bay, New York. 87th
Congress, 1st Session, House Document No. 138, U. S.
Government Printing Office, Washington, D. C. 42 p.
Great Sodus Bay Harbor is in Great Sodus Bay located on
the south shore of Lake Ontario. This interim report
considers channels and turning basin deepening and
enlargement, all in the interests of deep-draft bulk
cargo traffic. The purpose of the report is to determine
the need and the desirability of providing additional
navigation improvements at Great Sodus Bay Harbor to
accomodate the large bulk freight vessels anticipated
to be used in the future Great Lakes traffic.
117- Corps of Engineers. 1962a. Great Lakes harbors study -
Interim report on the Oswego Harbor, New York. 87th
Congress, 2nd Session, House Document No. 471, U. S.
Government Printing Office, Washington, D. C. 67 p,
Oswego Harbor, New York is located near the easterly end
of the south shore of Lake Ontario at the mouth of the
Oswego River. This Interim report considers the improve-
ment of Oswego Harbor, New York, in the interests of
deep-draft navigation traffic in both bulk and general
cargo. The purpose of the considered improvement is to
provide access channels and a turning basin of adequate
depths and dimensions to service terminal facilities in
the 1,600-foot reach immediately above the mouth of the
Oswego River.
118. Corps of Engineers. 1962b. Monthly bulletin of lake
levels. U. S. Army Corps of Engineers, Lake Survey
Detroit, Michigan. 1 sheet.
The U. S. Army Corps of Engineers monitors Great Lakes
levels monthly, records and then publishes the results
in a monthly bulletin. The bulletins for lake levels
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in past years are not available, however, a running
graphic monthly and yearly level tabulation is kept at
each branch office.
119. Corps of Engineers. 1965a. Water levels of the Great
Lakes - report on lake regulation main report.
U. S. Army Corps of Engineers, North Central District,
Chicago. 57 p + appendices.
The main report of a series of reports on the necessity
and effects of Great Lake level regulation. Paper
Includes water sources to the lakes, water outflows and
removal from the lakes and the economic benefits and
feasibility of lake regulation. (Univ. of Toronto, Great
Lakes Institute).
120. Corps of Engineers. 1965b. Water levels of the Great
Lakes - report on lake regulation appendix A -
hydraulics and hydrology. U. S. Army Corps of
Engineers, North Central Division, Chicago. 48 p. +
appendices.
Included in this article are data on Lake and land
drainage areas, tributaries, lake levels, climatology,
precipitation, runoff, ground water, evaporation, ice
retardation and lake water diversions. (Univ. of
Toronto, Great Lakes Institute).
121. Corps of Engineers. 1965c. Water levels of the Great
Lakes - report on lake regulation appendix B - lake
regulation. U. S. Army Corps of Engineers, North
Central Division, Chicago. 57 p. + appendices.
An in-depth discussion of the methodology involved in
the regulation of lake levels of the Great Lakes. Para-
meters discussed are runoff, precipitation, evaporation,
inflows and outflow. The effect of regulation of Lake
Ontario waters on the flow volume of the St. Lawrence
River is also discussed. The St. Lawrence receives
more water during high lake levels and less water during
low lake levels, than before the regulations came into
being. (Univ. of Toronto, Great Lakes Institute).
122. Corps of Engineers. 1965d. Water levels of the Great
Lakes - report on lake regulation - appendix C -
effect of lake regulation on shore property. U. S.
Army Corps of Engineers, North Central District,
Chicago. 43 p. + appendices.
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A discussion of the geology of the shore areas of the
Great Lakes is followed by an in depth discussion on
lake-level-shore erosion correlations. The erosion
parameter includes the effects of wind on the production
of waves and the effects of waves, winds, currents and
runoff on the shorelines of the lakes. An economic
evaluation of the regulation of water levels is also
presented in this paper. (Univ. of Toronto, Great Lakes
Institute).
123. Corps of Engineers. 1965e. Water levels of the Great
Lakes - report on lake regulation - appendix D -
effect of lake regulation on navigation. U.S.
Army Corps of Engineers, North Central District,
Chicago. 16 p. + appendices.
Experience on the Great Lakes has clearly demonstrated
that vessel operators have always taken advantage of
any increased depths provided for navigation. There
are today, and it is expected that there will continue
to be, vessels in the fleet which will be required to
load at reduced draft, except during times when the
levels of the Great Lakes are at high stages. Conse-
quently, lake level regulation altering the regimen of
lake levels by narrowing the range of extreme stages
that have been experienced, through a raising of the
lower levels and a reduction of the higher levels would
affect Great Lakes navigation.
The tentative lake regulation study plans developed in
this investigation are presented in detail in Appendix
B. There is one study plan for regulation of Lake Erie,
two study plans for regulation of Lake Michigan-Huron
and one for the regulation of Lake Superior. The
purpose of this Appendix D is to estimate the effect on
navigation of regulating the levels of Lakes Erie and
Michigan-Huron under the plans considered for these two
lakes. The appendix presents an evaluation of effects
on commercial and recreational navigation resulting
from the study plan for Lake Erie regulation. The
appendix develops estimates of the general magnitude of
effect on navigation of regulating Lake Michigan-Huron
under the study plans for that lake. (Univ. of Toronto,
Great Lakes Institute).
124. Corps of Engineers. 1965f. Water levels of the Great
Lakes report on lake regulation - Appendix F -
regulatory works. U. S. Army Corps of Engineers,
North Central District, Chicago. 24 p. +
appendices.
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To accomplish in some measure the several purposes of
lake regulation, two facilities must be provided at the
outlet of the lake that is to be regulated. First, the
discharge capacity of the outlet must be increased, so
that at times, larger releases of water from the lake
than would occur without regulation can be made in order
to reduce high lake levels. This requires channel
enlargements in the outlet river or the provision of
supplementary channels for augmentation of the outflow
capacity. Second, a gated control structure of structures
must be procided so that at other times smaller releases
than without regulation can be made in order to raise low
lake levels.
The tentative study plans considered in Appendix B for
the regulation of Lake Michigan-Huron and Lake Erie have
determined the critical combinations of regulated lake
levels and outflows that is necessary to provide for, in
order to make the considered regulation plans workable.
For Lake Michigan-Huron the regulatory works would be
provided in the St. Clair-Detroit River system; for Lake
Erie, in the upper reach of the Niagara River, Modifi-
cations studied for the regulation of Lake Superior were
considered on the basis of no changes to the existing
works in the St. Marys River. Similarlys no changes to
the works in the St. Lawrence River were contemplated in
the studies of this report. (Univ. of Toronto, Great
Lakes Institute).
125. Corps of Engineers. 1966. Red Creek, Genesee River
Basin, Monroe County, Mew York. 89th Congress,
2nd Session, Senate Document No. 107, U. S. Govern-
ment Printing Office, Washington, D. C. 62 p.
Red Creek, a minor tributary of the Genesee River, is
located near the northern end of the river basin and
has a drainage area of about 23 square miles, all in
Monroe County, New York. This report concerns improve-
ments in the Red Creek basin to satisfy present and
future needs for protection from the Genesee River over-
flows and from floods originating within the Red Creek
basin.
126 Corps of Engineers. 196?. Wilson Harbor, New York,
90th Congress, 1st Session, House Document No. 112,,
U. S. Government Printing Office, Washington, D. C.
59 P.
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Wilson Harbor is a small-craft harbor on the south shore
of Lake Ontario at the mouth of the East Branch of
Twelvemile Creek in New York. Just before entering Lake
Ontario, the East Branch of Twelvemile Creek flows through
a shallow embayment known as Tuscarora Bay. This report
considers modification of the existing Federal project to
provide for a suitable channel and maneuvering area in
Tuscarora Bay, and certain changes in the present require-
ments of local cooperation, in the interest of small-boat
navigation.
127. Corps of Engineers. 1968. Hamlin Beach State Park, New
York. 90th Congress, 2nd Session, House Document No.
358, U. S. Government Printing Office, Washington,
D. C. 53 p.
Hamlin Beach State Park comprises about 2 1/*J miles of
shore in the central part of the southern shore of Lake
Ontario. It is located in the town of Hamlin in Monroe
County, about 20 miles west of Rochester.
This report considers the advisability of Federal improve-
ment to provide a small-boat harbor at Hamlin Beach State
Park, New York. Such a harbor would supplement the pro-
gram of small-craft harbors. This presently authorized
chain of small boat harbors is primarily for the larger
cruising recreational craft. The principal consideration
given in the present report is to the need for an inter-
mediate harbor to serve the smaller cruising craft, and
to provide a base for additional boats.
128. Corps of Engineers. 1969a. Great Lakes and St. Lawrence
Seaway navigation season extension. Department of
the Army, Detroit District, U. S. Army Corps of
Engineers, Detroit, Michigan. 76 p., 22 maps +
plates.
A review of world wide experience in ice navigation and
ice modification techniques indicates that present tech-
nology is sufficiently advanced to make winter operation
on the Great Lakes - St. Latvrence Seaway system physically
feasible. The extent to which winter operation should be
undertaken at this time, and the economic feasibility for
either limited or full 12 month extension, cannot be
determined on the basis of the limited investigations made
in this study. However, estimates or prospective traffic
and benefits demonstrate a magnitude of economic potential
which clearly Indicates need for further investigation
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and development. The feasibility study, therefore,
recommends both immediate and long-range objectives for
development of an extended navigation season on the Great
Lakes - St. Lawrence Seaway. (Canada Centre for Inland
Waters).
129. Corps of Engineers. 1969b. Great Lakes shoreline damage.
U. S. Army Corps of Engineers, North Central Division,
General Information Pamphlet (Chicago). 21 p.
Part I is a history and background discussion of lake
levels, causes of fluctuations and most Important,
effects of lake level changes on shorelines. Part II
discusses the role of Federal and State Governments in
various activities and responsibilities on the Great
Lakes related to water and shore areas. It includes
information on available data and sources of such data.
Part III is a brief discussion of several emergency type
remedial measures, estimates of thin cost and general
statements on their applicability to various typical
situations.
130. Corps of Engineers. 1970a. Beach erosion study of
east end of Oneida Lake, N. Y. Prepared for the
State of New York Department of Environmental
Conservation, Division of Water Resources. U. S.
Army Corps of Engineers, Buffalo, N. Y. Unnumbered.
Oneida Lake Is located in central New York about 12 miles
north-easterly of Syracuse, New York. The purpose of this
beach erosion control study is to investigate the causes
of reported loss of beaches and subsequent erosion damage
to the shore from wave action.
131. Corps of Engineers. 1970b. South shore of Lake Ontario,
Fort Niagara State Park. 91st Congress, 2nd Session,
House Document No. 91-319. U. S. Government Printing
Office, Washington, D. C. 56 p.
Fort Niagara State Park is located on the south shore of
Lake Ontario at the mouth of the Niagara River. The pur-
pose of this study is to develop plans for the protection
and improvement of the easterly 4,000 linear feet of the
Lake Ontario frontage of Forfc Niagara State Park. In
addition to providing protection against erosion from
wave action, the State of New York wishes to restore and
improve the beach for use as a public bathing beach. The
economic Justification of considered improvements and the
extent of the Federal interest and participation in their
cost are also to be determined.
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132. Corps of Engineers. 1971a. Environmental statement -
Oswego steam station - Unit 5, Niagara Mohawk Power
Corporation. U. S. Army Corps of Engineers, Buffalo,
New York. 85 t>.
Data on the general lake conditions at the Oswego Steam
Station (Niagara Mohawk Power Corporation). Parameters
discussed in relation to physical environment are:
Topography Surface Water - dimensions, runoff,
Geology precipitation, lake levels,
Ground Water currents, thermal gradients
133- Corps of Engineers. 1971b. Great Lakes region inventory
report national shoreline study. U. S. Army Corps
of Engineers, North Central Division, Detroit,
Michigan. 221 p.
This report concerns erosion and the need for protection
of the shoreline zone of the United States portion of
the Great Lakes. The shoreline zone or shorelands include
the land, water and the land beneath the water in close
proximity to the Great Lakes shoreline.
Section 10 concerns the State of New York and includes 3
subsections on Lake Ontario - the Lake Ontario West
Planning Subarea, the Lake Ontario Central Planning Sub-
area and the Lake Ontario East Planning Subarea. Each
subarea includes a shoreline description, Information on
erosion and flooding history and solutions to erosion
damages.
131*. Cronan, D. S. and R. L. Thomas. 1970. Geochemistry of
ferromanganese oxide concretion in Lake Ontario.
Proceedings, Meeting Geological Society of America,
Milwaukee, Wisconsin, p. 529.
A large deposit of ferromanganese oxide sands and
scattered manganese nodules extend 210 km. east from
Toronto with a maximum width of 20 km. and thickness
of 4 cm. The nodule's zinc, nickel, copper and cobalt
contents are lower than those found in sea water.
Analysis of bottom water associated with the concretions
show that manganese, iron, nickel, cot>t>er, lead and zinc
are highest in concentration indicating the upward
diffusion of these elements from buried sediments might
be contributing to the concretion formation.
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Csandy, G. T. - See: C. R. Murthy, No. 276.
35. Csandy., G. T. 1964. Turbulence and diffusion in
the Great Lakes. Great Lakes Research Division,
Publication No. 11, Univ. of Michigan, pp. 326-
339.
In continuing experimental investigations of turbulent
diffusion in the Great Lakes, further data have been
collected, particularly on verticle diffusion and
diffusion in a current which steadily changes direction
("swinging" current). Also a comparison could be made
between diffusion in Lake Huron and Lake Erie, western
basin; The low value of verticle diffusity reported
before were confirmed, and the extreme influence of
thermal stratification on verticle diffusion was demon-
strated. Diffusion in a swinging current was found to
be considerably more rapid than in a steady one, the
effective diffusity (so far as such a concept is useful
in that situation) increasing by a factor of 2-5.
36. Csandy, G. T. 1967. Large scale motion in the Great
Lakes. Journal of Geophysical Research. 72(16):
4151-4162.
Large scale motion in the Great Lakes consists of three
motions.
1. Baroclimic Coastal Jets during summer
stratification.
2. Slow counterclockwise rotating Internal
waves of a period many times the helf-
pendulum day.
3. Surface and Internal seiches rotating in
either direction and having a period of
at most several hours (surface modes) or
up to within a small fraction of the
inertial period (internal modes).
17. Csandy, G. T. 1968a. Simple analytical models of
wind driven circulation in the Great Lakes. Pro-
ceedings llth Conference Great Lakes Research.
pp. 371-384.
The important dynamical factors in determining large-
scale water movements in the Great Lakes sppear to
be: (1) wind stress; (2) the constraint of continuity
imposed by the shores of a closed basin, (3) Coriolis
face - may be assumed constant for a basin as large as
the Great Lakes basin.
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Summer density stratification and depth variation also
exert on controlling influence on the current patterns.
Large scale motion features include (1) coastal jets,
(2) thermocline movements, (3) current rotation patterns.
138. Csandy, G. T. 19680. Wind driven circulation in the
Great Lakes. Journal of Geophysical Research.
73(8): 2579-2589.
Simplified models of wind-forced motions are considered
in a two-layer circular basin "model great lake" Intro-
duced In an earlier paper. Under summer conditions,
when a thermocline Is present, both a uniform, steady
wind and a uniform tirind varying periodically In* time
produce a frictlonless lake response characterized by
strong boundary currents and pronounced thermocline
movements In the shore zone. The length scale deter-
mining the widths of this shore zone is the "radius of
deformation," typically three miles. Observations on
Lakes Huron, Michigan and Ontario show such motions to
be present near the shores.
139. Csandy, G. T. 1969. The coastal Jet project. Depart-
ment of Mechanical Engineers, Univ. of Waterloo.
18 p.
During the summer of 1969, an extensive series of current
and temperature measurements in the coastal zone of Lake
Ontario, near Oshawa, Ontario, were conducted. The main
scientific objective of the work was to determine
whether or how often the theoretically predicted "coastal
Jet" phenomenon was In evidence In this area, following
some indications during the 1968 season to the effect
that such Jets were possibly present on certain occasions
near Douglas Point, in Lake Huron. A second objective
was to further prove the practical value of such observa-
tions by means of the relatively inexpensive "flag
station technique" which provided useful results during
the 1968 season. The Canada Centre for Inland Waters,
Burlington, Ontario, again supported the work.
The 1968 observations could be described as essentially
a "feasibility study" for two different observation
techniques,in the course of which the flag-station
technique emerged as superior. The evidence for or
against Coastal Jet near Douglas Point remained meanwhile
inconclusive, mainly on account of a lack of continuity
In the observations. In order to Identify a given current-
pattern as a "coastal Jet" it Is necessary that It show
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persistence at least for several inertial periods. The
1969 Oshawa observations were reasonably useful In this
regard yielding a fairly complete coverage of the period
May 15-July 31, on 48 days of which observations were
carried out, giving on most days one cross-section of
current and temperature, on some days two. Even though
not all sections were complete, the net output represents
an acceptably high yield of data in the light of the
instrumentation experienced.
Generally speaking, the results obtained show a fascina-
ting wealth of complex phenomena. However, not a single
Instance of "coastal jets" (» persistent barocllnic
currents a few miles wide) could be uncovered, although
stratification was pronounced in the second half of the
experimental period. As to the flag-station technique,
its practical value again became evident, although we
also learned of some of its limitations. Instrument
(current metering) problems were again fairly serious,
but the experience gained will probably prove valuable
in later seasons. (Canada Centre for Inland Waters).
140. Csandy, G. T. 1970. On the equilibrium shape of the
thermocline in a shore zone. In: Coastal Jet
Project, 1970. Canada Centre for Inland Waters.
p. 7.
The typical spring thermal regime of Lake Ontario shows
a thermocline surface of either a "wedge" or of a "lens"
shape persisting in the shore zone for a considerable
period. The summer regime is characterized by frequent
uptilts or downtilts on the thermocline, with an
amplitude comparable in the shore zone to the equilibrium
depth of top or bottom layers. These observed facts are
explained in terms of a simple theory based on the post-
ulates of geostrophic flow and velocity distributions
calculated for a constant-depth shore-zone model exhibit
many of the observed characteristics of the spring and
summer regimes, (Canada Centre for Inland Waters).
Csandy, G. T. 1971- On the equilibrium shape of the
thermocline in a shore zone. Unpublished paper
presented at the 3.4th Conference Great Lakes Research,
Toronto. April 19-21, 1971. p. 192.
The typical spring thermal regime of (say) Lake Ontario
shows a thermocline surface of either a "wedge" shaped
or of a "lense" shaped cross section, the warmer water
being confined to the shore zone for a considerable
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period (of order two months). The summer regime is
characterized by frequent uptilts and downtilts on the
thermocline in the shore zone, or relatively large ampli-
tude, so that the thermocline may come to intersect
either the free surface or the bottom of the lake. Once
established, such uptilts or downtilts usually persist
for at least several days.
The density distribution implied by the above shapes of
the thermocline surface cannot be in static equilibrium
and the question arises, what kind of dynamic equili-
brium enables these distribution to persist for
considerable periods. The view has been expressed by
Rodgers and others that, at least in the case of the
spring regime, the horizontal movement of warm water is
checked by mixing at its lakeward edge, but no quantita-
tive theory to this effect has been proposed. An
alternative, and as it turns out rather more attractive,
explanations is that the observed temperature distribu-
tion is in geostrophic valance. In support of this
argument the dynamic behaviour of a simple shore zone
model is investigated analytically. In a constant depth
basin a portion of the water closest to the shore is
suddenly heated. Inertial oscillations ensue, and it is
also likely that a considerable fraction of the available
potential energy appears as kinetic energy of geostrophic
motions. If the energy of these is more than half of the
available energy, a wedge-shaped equilibrium thermocline
develops. A lenss-shaped thermocline is also found to be
possible and requires somewhat less energy in geostrophic
motions.
The theory is based on the conservation of (potential)
vorticity, friction being neglected. Without postulating
"small" thermocline displacements a simple differential
equation is obtained (for either spring or summer regime)
the solutions of which exhibit many of the observed
thermocline characteristics.
142. Csandy, G. T. and B. Fade. 1971. Coastal current
regimes in Lake Ontario, Abstract of paper pre-
sented at 14th Conference Great Lakes Research.
P. 47.
Originally promped by a desire to search for the
theoretically predicted "coastal jets," an extensive
series of observations on currents in the coastal zone
near Oshawa, In Lake Ontario, have been carried out
during 1969 and 1970. A general characteristic of the
water movements is the great spatial variability.
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Other characteristic features of the observed water
movements are: 1. the level of kinetic energy in the
currents, and 2. the shape of the associated thermo-
clinesurface. These appear to go through seasonal
changes.
Csandy, G. T. and H. G. Fade. 1970. The coastal Jet
project. Department of Mechanical Engineering,
Univ. of Waterloo, Ontario. 20 p.
Current and temperature cross-sections reveals the
following features:
1. Spring regime. This is characterized by a thermo-
cline surface ringing the entire lake and isolating the
\varmer water in a nearshore band, the cross-section of
which shows either a "wedge-shaped" or a "lens-shaped"
thermocllne. Maximum baroclinlc currents calculated from
the temperature distribution (by the geostrophic approxi-
mation) in this regime are of the order of 5 cm/sec,
while maximum observed velocities are several times
higher (order 20 cm/sec) and are also poorly correlated
with the temperature distribution. The current pattern
changes from day to day, the fixed current meters showing
the occasional presence of inertial oscillations and
other unsteady motions. All these motions are, however,
mostly confined to narrow spatial regions, much of the
surveyed i/ater mass being nearly stagnant most of the
time during the spring period.
2. Summer regime. The thermocline surface is now con-
tinuous across the lake and often shows an uptilt or a
downtilt near the shore. Calculated baraclinic velocities
are now higher, of the same order as observed velocities
but the two are still poorly correlated. The current
pattern still changes from day to day and inertial
oscillations are prominent. The total kinetic energy of
the motions is appreciably higher than during the spring,
although the bottom layers are still nearly stagnant most
of the time.
3. Pall regime. The thermocline behaves much as during
the summer, although it is located rather deeper. More
pronounced and persistent bands of current appear,
drifting inward or outward from day to day. The total
kinetic energy is very much greater than during spring
or summer. Also thermocline uptilts and downtilts are
more striking and persistent.
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Viewing the Coastal Jet project as a feasibility study
for IPYGL work, we may perhaps claim the following:
(a) Observations by means of the flag-station technique
are well worth collecting, because no other method so
far known provides comparable detail on the fascinating
complexity of coastal lake currents. Certainly no prac-
tical number of anchored current meters would provide
equivalent coverage.
(b) The technique is relatively inexpensive (certainly
in comparison with projects requiring larger vessels).
A realistic cost estimate is $15,000 per coastal chain
per alert period. (We note that this year's contract
price did not cover all our expenditures).
In the following, the experimental technique and any
difficulties experiences are described briefly, followed
by a presentation of the observed data. The data are
also illustrated by temperature and current cross-sections,
which are largely self-explanatory and demonstrate the
points breifly made above. A more detailed analysis of
the dynamic factors involved in the observed current
distributions may be found in a recent paper of which the
abstract is attached, and in a second paper now under
preparation. (Canada Centre for Inland Waters).
Czapski, U. H., R. Stewart and J. T. Scott, 1970. An
estimate of the air-water balance near west Nine
Mile Point, Lake Ontario. Proceedings 13th Confer-
ence Great Lakes Research, p. 798-810.
A preliminary study of the energy imput into the atmos-
phere from a small area of the lake surface near Nine
Mile Point is reported. The installation of two power
stations plus other large heat dissipators (Aluminum
Plant), makes this part of the lake an interesting
target for energy budget studies. In order to assess
the basic unaltered heat fluxes, standard energy budget
and aerodynamic techniques are applied using previously
published data and field data obtained by the authors in
the summer of 1969. Estimates of total latent energy
and sensible energy fluxes and the sum of these are
obtained from calculations of heat advection and heat
storage change in the water, and from dry and wet bulb
temperatures, wind speeds and radiation measurements.
Assuming that the spread of warm surface waters of
thermal effluents from the power station is similar to
the known spread of Oswego River effluent as indicated
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by the data of infrared surveys, estimates of latent
and sensible heat flux, in excess of normal from the
lake to the atmosphere, are presented as a function of
area.
145. Davies, J. A., M. Nunez and P. J. Robinson. 1970.
Radiation measurement over Lake Ontario and the
determination of emissivity. Abstract of paper
presented by McMaster University, Department of
Geography. p. 10.
Prom July to November 1969, a group from McMaster Univ-
ersity, in cooperation with the Canada Centre for Inland
Waters, carried out a radiation flux study over Lake
Ontario. An instrumented tower was installed at the
western end of the lake in shallow water (4m deep) about
400 m from the shore.
The study has four main aims:
1. To define the short-term (hourly) and long-term
(daily) variation in the components of the radiation
balance at an air-lake interface and their relationships
with environmental factors.
2. To examine the feasibility of empirical prediction
of these components using relatively simple meteorolo-
gical predictors.
3. To assess the performance and suitability of
available radiation sensors in meteorological studies
over lakes.
4. To determine relevant surface parameters, such as
albedo and emissivity, which might be useful in analyzing
data from remote sensing.
The first report is concerned with the approaches to
radiation flux measurement and calculation used in this
study. The first part deals with the sensors used, the
principles of their operation and their use for specific
measurements. In the second part, field methods for
determining surface emissivity and temperatures are
described and a preliminary discussion of the results
are presented.
The second report presents the radiation flux data
collected at a tower site in Lake Ontario from July to
November 1969. The radiation fluxes are listed for
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half-hourly periods and as 24-hour totals for each day
from July 1 to November 18, 1969.
146. Day, P. C. 1926. Precipitation in the drainage area
of the Great Lakes, 1875-1924. Monthly Weather
Review. 54(3): 85-106.
The average rainfall for the Great Lakes drainage area
from 1875 to 1924 was about 32 Inches per year with an
increase in precipitation from north to south.
Prom 1875 to 1885 the precipitation was unusually heavy.
Prom 1917 to 1924 the amount of water reaching the lakes
was decreased due to previous extensive logging.
147. Deane, R. E. 1963. Limnological and meteorological
observation towers in the Great Lakes. Limnology
and Oceanography. 8(1): 9-15-
Slx limnological and meteorological single-shaft towers
of 4 inch pipe were installed in three of the Great
Lakes by the Great Lakes Institute, University of Toronto,
The towers were of two types; a shallow water tower for
depths of less than 60 ft. where the base of the tower
rested directly in the lake bottom, and a deep water
tower supported by a bouyancy tank 25 ft. below the lake
level. A platform on the towers, situated 8 to 12 ft.
above lake level, gave a suitable base of house limnolo-
gical and meteorological instruments and recorders. The
platform and upper tower section were designed for easy
removal and reinstallation.
Deck, B. L. - See: R. C. Bubeck, No. 47.
148. DeCooke, B. G. 1967. Control of Great Lakes water
levels. U. S. Army Corps of Engineers, Detroit,
Michigan. Lake Survey, MP 67-1. 9 p.
The four natural hydrologic factors - precipitation, run-
off, groundwater and evaporation - along with the inflow
from the lake above are the major factors In determining
lake levels. Because of the large natural variations in
water supply, It is impracticable to regulate any of the
lakes to maintain a constant elevation. This would
require enlarging the lake outlets to facilitate a dis-
charge capacity equal to the largest monthly supply to
the lake. In some cases, this would double the capacity
of the present outlet. Pumps would have to be installed
of offset any negative supply when evaporation from the
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lake surface is greater than the amount of water
supplied. The more rational approach is to research
regulation of extreme water levels using the same
techniques. (Canada Centre for Inland Waters).
DeCooke, B. G. 1968a. Great Lakes regulation. Pro-
ceedings llth Conference Great Lakes Research.
pp. 627-639.
The paper presents a brief description of the physical
characteristics and of the hydraulics and hydrology of
the Great Lakes system, along with a summary of regula-
tion studies conducted during the past half century.
The technique employed to develop current operational
regulation plans on the lakes and the latest International
studies for regulation of the entire Great Lakes, and
problems of special interest encountered therein are
described. Discussion of the derivation of basic data
(e.g. levels, flows, supplies, etc.), uniform base of
comparison employed in these studies, requirements of
regulation, various approaches to regulation, and methods
of evaluating results are included. (Canada Center for
Inland Waters).
150. DeCooke, B. G. 1968b. Regulation of Great Lakes levels
and flows. U. S. Army Corps of Engineers, U. S.
Lake Survey, Detroit, Michigan. MP 68-8. 26 p.
This paper presents a brief description of the physical
characteristics, as well as hydraulics and hydrology, of
the Great Lakes system. Included are tables of average
lake levels, outflows, runoff, precipitation and evapora-
tion. The rule and limitation approach to regulation
plan development (a plan tailored to the past sequence
of water supplies) and the probabilistic and stockastic
approach (a plan which gives consideration to the varia-
bility of future water supplies) are described and
compared. The paper includes a description and samples
of regulation plans presently in operation on Lakes
Superior and Ontario. The author concludes that it is
extremely difficult to Improve on the natural regulation
of the system. However, from an engineering standpoint
regulation of the entire system is feasible, but has not
been economically justified to date.
151. DeCooke, B. G. and E. Megerian. 1967. Porcasting the
levels of the Great Lakes. U. S. Army Corps of
Engineers, U. S. Lake Survey, Detroit, Michigan.
MP 67-2. 7 p.
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A description is given of the U, S. Lake Survey method
of forcasting Great Lakes water levels. The method, in
general, consists of determining a level for each month
of a 6-month forcast period on each of the Great Lakes by
routing a predicted volume of water (Net Basin Supply) to
each of the Great Lakes Basins. The technique employed
in prediction of the volume of the water consists of
using multiple linear regressions based on U. S. Weather
Bureau precipitation and temperature data as precitors
for the first month and trend predictors for the second
through the sixth month. This technique results in for-
casting of lake levels on the average from 15 to 40$
closer to the recorded lake levels in comparison with the
technique that utilizes the long term average volume of
water as the basis of projection.
152. Denison, N. 1898. Periodic fluctuations of the Great
Lakes. Monthly Weather Review. 26: 261-262.
Two self recording depth gauges were used to determine
lake fluctuations in Toronto region of Lake Ontario.
Lake fluctuations were measured and two types identified:
1. larger undulations of about 20 minutes.
2. smaller undulablons of about 10 minutes.
It was stated that the lake' level never reaches a
stationary level.
153- Denison, P. J. and P. C. Elder. 1970. Thermal inputs
to the Great Lakes, 1968-2000. Proceedings 13th
Conference Great Lakes Research, pp. 811-828.
A survey of expected man-made thermal imputs to the
Great Lakes system from electric generating plants,
steel mills and municipal waste treatment plants for
the period 1968-2000 has been completed. The present
thermal imput of 9.98 x 10 Btus. per hour of the total
lake system is expected to rise more than 11 times to
114 x 10 Btu. per hour by the year 2000. As an indica-
tion of the magnitude of this projected thermal input,
the contribution to Lake Ontario in 2000 A.D. will amount
to 6% of the total annual natural heat storage in the
Lake.
Dewey, C. 1838. Temperature of Lake Ontario. American
Journal of Science. 33: 403-405-
Lake Ontario fails to freeze in the winter due to its
great water volume (depth and surface volume). In late
winter, some ice forms but is quickly broken up by
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strong winds. The shoreline area is cooler in the winter
months and warmer in the summer. The great depth in the
lakes center basins resist thermal change.
155. Dewey, C. l839a. On the polished limestone of Rochester.
American Journal of Science and Arts. 37: 240.
The occurrence of several areas of polished limestone
in the Rochester area indicate a strong frictional agent
working or running over these large rocks for long periods
of time. Several hypothesis are presented but no conclu-
sions are drawn.
156. Dewey, C. l839b. On the temperature of Lake Ontario.
American Journal of Science and Arts. 37: 242-243.
A repetition and varification of previous work on a
surface temperature study of Lake Ontario from the
Genesee River to Coburg. The effect of water depth in
the central basin on the surface temperature of the lake
is Implied. The center lake area is cooler in summer and
warmer in winter due to the large water masses thermal
resistance.
157. Dewey, C. 1843. Straie and furrows of the rocks of
western New York. American Journal of Science and
Arts. 44: 146-150.
Article reveals the location of areas in Western New York
where large furrows and strale appear in large rocks.
These are believed to be produced by glaciers and icebergs
along with strong water currents. The strong currents
would also be responsible for the movement of many large
boulders.
158. Dewey, C. 1859. The varying level of Lake Ontario.
American Journal of Science (2nd series). 27: 398-
399.
A general discussion of the degree, causes and effects of
lake variation is presented. Causes can be inflow-outflow
volume ratios, precipitation-evaporation ratios and atmos-
pheric pressure. Lake level data are presented and
discussed.
Digman, Ralph E. - See: F. K. Mack, No. 257.
Diment, W. H. - See: R. C. Bubeck, No. 47.
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59. Dohler, (}. C. and R. J. D. MacKenzie. 1969. A discussion
on the interpretation of high and low water datum
planes in the Great Lakes. Proceedings 12th Con-
ference Great Lakes Research, pp.
There is a growing and continuing requirement for more
precise definitions of the various levels of the Great
Lakes, Every sector of the Great Lakes Basin Community
is affected, sooner or later by the lake levels. The
purpose of high and low water datum are examined and
defined, and the criteria which could meet these require-
ments are established. All available water level data
are analyzed and techniques developed for the selection
of appropriate datum planes.
160. DolLen, Bernard H. 19^0. Water resources of the Clyde
an 3 Sodus Bay quadrangles. New York State Museum
Bulletin No, 320. 159-171 p.
Included in this article is a discussion of the surface
waters of the two quadrangles which Includes Lake Ontario
and its tributaries.
161. Donato, R. J. and G. D. Hobson. 1968. Transit sonar
measurements In Lake Ontario off the mouth of the
Nlapard. River, Proceedings llth Conference Great
Laker- Research, pp. 179-187.
Records obtained from a Kelvin Hughes Transit Sonar
Instrument have been spliced together and a comparison
made between amplitude of signal and bottom samples to
identify oottom materials. Supplementary data from
hydt-Oj-rr-aphlc charts enables a fairly comprehensive
interpretation to be made.
r~v
There is virtually no penetration into the sediments by
the sound beam from the sonar, penetration being about
1 inch into the very recently deposited sediment. The
recorded Intensity of the recorded beam Is dependent
both upon bottom topography and the composition of the
sedirnert cf the water bottom interface.
One profile was surveyed along about five miles of the
Niagara River above Niagara-on-the-Lake. This record
shows the strong reflection from the east bank of the
river, as well as the strong indication of a mud and sand
bottom. Some prominent ridges are revealed which, from
their shadow region may be 8-10 ft. high. Twenty other
orofiles wore surveyed in Lake Ontario off the mouth of
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the Niagara River. These records are shown with an
interpretation of the bottom materials and a. correlation
of data front coring stations and hydrographic charts.
Dragert, H. - See: T, L. Richards, No. 313.
162. Drake, R. L. , D. V. Anderson and C. P. Peterson. 1971.
Explanation of and preliminary results from a meso-
scale model of Lake Ontario, Unpublished paper
presented at the 14th Conference Great Lakes Research
Toronto, April 19-21, 1973- pp. 177-178.
A mesoscale model for the study of lake-effect storms
over Lake Ontario is being constructed and tested. The
model being; employed is a modification of the Lavoie
Lake storm model. The principal quantities which are
obtained from this model are the horizontal wind com-
ponents, potential temperature and humidity in an
adiabatic layer, and the height of the inversion layer.
Auxiliary quantities are the average vertical velocity
and the amount of rain or snow falling to the ground.
163. Drummond, A. T. 1889- Some Lake Ontario temperatures.
Nature. 40: 4l6.
The surface temperatures of Lake Ontario vary in June on
an average of 1 to 3°C. The thermal gradients, as depth
Increase vary to a much greater extent. The air-water
temperature Imbalance produces notlcable climatological
effects in fall and spring, but not summer and wnter due
to the lesser degree of variance between temperatures at
this time.
164. Dunn, B. 19&7 Maximum known stages and discharges of
New York streams through 1967. U. S,Geological
Survey Bulletin 67. 57 p.
This report represents a compilation of all known maximum
stages and discharges in the files of the Geological
Survey, including a limited amount of data furnished by
other Federal, State and Private Organizations. The data
are tabulated under the heading of the major river or lake
basin in which the stream Is located,
Dutka, B. J. - See: A. S, Menon, No. 269.
Dutka, B. J. - See: J. N. Vanderpost, No. 421.
Eadie, W. J. - See: G. E. McVehil, No. 266.
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Elder, F. C. - See: P. J. Denison, No. 153.
165. Elder, P. C. and R. K. Lane. 1970. Some evidence of
meteorological related characteristics of lake
surface temperature structure. 13th Conference
Great Lakes Research, pp. 3^7-359.
The surface temperature structure of western Lake Ontario
was mapped using an infrared scanner and an infrared
thermometer on four days during a six-day period in May
1969. Spatial resolution of the infrared scanner gave
extreme detail in the surface temperature structure and
the repetition on closely spaced days allowed determina-
tion of rates of change and persistence of the surface
temperature features. Features such as the Niagara River
plume were persistent throughout the six-day period.
However, very detailed patterns showing evidence of
banded, cellular and rotational structure were observed.
It is shown that these features are associated with
existence of a convectively unstable layer near the
surface caused by surface heating of water at less than
the maximum density temperature. These surface features
are shown to be present only in the near absence of
mechanical mixing and are, therefore, related to the
prevailing meteorological conditions. (Key words:
air-water interactionj instruments and techniques; Lake
Ontario). (Canada Centre for Inland Waters).
Eryuzlu, N. E. - See: R, L. Pentland, No. 296.
166. Pairchild, H. L. 1893. The geological history of
Rochester, New York. Proceedings Rochester Academy
of Science. 2: 215-223.
Using a 3000 ft. core sample drilled in Rochester, an
analysis is made of the geological history of the area.
By correlating certain rock strata by location and com-
position, with previously known information on
environmental characteristics producing the rock strata,
a rather detailed picture of the history is produced.
The author follows through several areas of glacial
deposits, lake and stream deposits with reference to
duration and depth.
167. Fairchild, H. L. 1928. Geologic story of the Genesee
Valley and Western New York. Scrantom's Company,
Rochester, New York. 216 p.
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Geological history believed to be responsible for the
formation of Rochester Canyon, Portage and Mt. Morris
Canyons. Includes glacial periods and various lake and
river stages involved.
168. Falrchild, H. L. 1932. New York moraines. Geological
Survey of American Bulletin. 43: 627-662.
This article contains data of the following subjects:
moraine descriptions and belts, the Susquehanna Valley
kames, the Escarpment, Valley Heads Moraine, the Hamburg-
Batavia-Victor Moraine, the deglaciation interval, the
kame areas-Waterloo-Auburn Moraine-Second Lake Warren,
the Albion-Rochester Moraine, the Oswego Moraine, the
conflict of Lake and glacier, valley lobations and ice
front reentrants movement of the Ontario Ice Body,
Syracuse district-drainage control, Mohawk Valley loba-
tions, Catskills and Adirondacks drift and mountain
glaciers.
Penlon, M. - See: D. R. Landsberg, No. 2^3.
Penlon, M. - See: J. T. Scott, No. 3*»3.
Pisher, D. W. - See: J. G. Broughton, No. 39.
169. Pisher, Donald W. I960. Correlation of the Silurian
rocks in New York State. New York State Museum
and Science Service Geological Survey, Map and
Chart Series No. 1. 1 sheet.
Contains a large map and accompanying tables of the
Silurian rocks in New York State. The various geolo-
gical eras are discussed along with geology, strati-
graphy, evolution, erosion and topography.
170. Pisher, Donald W. 1962a. Correlation of the Cambrian
rocks in New York State. New York State Museum
and Science Service Geological Survey, Map and
Chart Series No. 2. 1 sheet.
Contains a large map and accompanying tables of the
Cambrian rocks in New York State. The various geolo-
gical eras are discussed along with geology, strati-
graphy, evolution, erosion and topography.
171. Pisher, Donald W. 1962b. Correlation of the Ordovician
rocks in New York State. New York State Museum and
Science Service Geological Survey, Map and Chart
No. 3« 1 sheet.
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A large Geological map and discussion involving the
Ordovician rocks of New York State, their subdivisions
and correlations and characteristics of each.
172. Pisher, Donald W. , Y. W. Isachsen, L. V. Rlckard, J. G.
Broughton and T. W. Of field. 1962. The geology
of New York State. New York State Museum Map and
Chart Series No. 5. 10 sheets.
Large topographical, geological maps of New York State.
Counties included along Lake Ontario and the Niagara
River include: Erie, Niagara, Orleans, Monroe, Wayne,
Oswego, Je-ferson and St. Lawrence.
173. Forrester, G. C. 1928. The falls of Niagara. D. Van
Nostrand Company, Inc., New York City, New York.
P.
Evolutionary of geological information on the falls of
Niagara, the Niagara River, the shorelines along the
river, and the Niagara Escarpment. Includes extensive
data on glaclatlon, erosion, rivers and changes in the
general geography of the area.
Portin, J. P. - See: T. L. Richards, No. 314.
Fricbergs, K. S. 1965. Beach stabilization in the
Toronto area. Unpublished thesis for registration
in the Assoc. of Professional Engineers of Ontario.
110 p.
Ever since the first settlers increased the growth of
the Toronto peninsula by clearing the Scarborough Bluffs ,
the local beaches have undergone profound man-made
changes. Construction of groynes, dredging for landfill
or harbor entrances, power plant discharges and land
reclamation, as well as ability to control the lake levels
have been the main agencies in shoreline movement.
A wave rose reveals that the prevailing south-westerly
winds are almost incapable of rising ten foot waves,
while the easterly storms may produce waves of the
12-14 foot class.
The summer months from May to October are found to be
relatively calm. In winter months there are storms
capable of reducing the man-made beaches of the order
of a hundred feet in less than two days. Hence, any
landfill program in the open lake initiated for pro-
tection of unsuitable material (garbage) should have a
clean fill-to-garbage ratio of at least three to one.
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175. Fricbergs, K. S. 1970. Erosion control in the Toronto
region. Proceedings 13th Conference Great Lakes
Research, pp. 751-755.
The Toronto Island, a recurved sandspit that protects
the Toronto Harbour, has been formed by littoral drift
derived from the eroding Scarborough Bluffs nearby.
Increasing stability of the Bluffs and dredging for fill
and harbour entrances have combined to starve the Island
markedly. A number of protective measures appear to have
given only temporary relief and/or compounded the problem
elsewhere.
Availability of construction excavation material from the
city central section has enabled the Harbour Commissioners
to reclaim economically for the growing harbour 90.6
hectares from the lake in I1! years. Now a breakwater,
built of the same material along the 10 m contour is three
km long and shelters the developing outer harbour.
Slope adjustment goes on for several years and may require
renurlshment. For equal exposure, steepness depends on
median size and gradation. The lateral movement of the
material Is constricted by protruding points built of
larger sizes.
176. Gannon, J. E. and A. M. Beeton. 1969. Studies on the
effects of dredged materials from selected Great
Lakes Horbours on plankton and benthos. Center
for Great Lakes Studies, Univ. of Wisconsin,
Milwaukee. Special Report No. 8. 82 p.
Sediment from the harbors of Buffalo, New York; Calumet,
Illinois; Cleveland, Ohio; Great Sodus Bay, New York;
Green Bay, Wisconsin; Indiana Harbor, Indiana; Milwaukee,
Wisconsin, Rouge River (Detroit), Michigan; and Toledo,
Ohio were analyzed for COD, NH-,-Mp, organic N2, POn-P
and volatile solids. Gross observations and particle
size analysis data are also tabulated.
177. Gibbes, L. R. 1857. Remarks on Niagara Falls. Proceed-
ings of the American Association Advancement of
Science, 10th Meeting, Albany, New York. pp. 69-78.
The evolution of Niagara Falls has taken place due to
water erosion at a very slow pace from the Bluffs at
Lewiston to its present site. The falls must have
developed into two falls upon approaching Goat Island
with the recent erosion of the Canadian Falls, nearly
three times as fast as the American Falls.
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Glese, G. L. - See: W. G. Weist, No. 1*31.
178. Gilbert, B. K. and J. C. Kammerer. 1965. Summary of
water resources records at principal measurement
sites in the Genesee River basin through 1963-
U. S. Department Interior, Geological Survey,
Bulletin 56. 55 p.
This report is a tabular summary of more than half a
century of water measurements (mainly streamflow) in
the Genesee River basin by the U. S. Geological Survey,
usually in cooperation with State and other Federal
agencies. The range in streamflow Is from less than 1
cfs (cubic feet per second) during dry-weather periods
on five tributaries measured, to a flood flow on the
Genesee River Itself of more than 55,000 cfs, near Mt.
Morris on May 17, 1916. The average flow of the
Genesee River at Rochester is 2,738 cfs, equal to a
basin-wide runoff of 1.1 cfs per square mile, or 15
inches of water annually.
Ground water levels measured in three wells for more
than ten years, show no long-term decline of the water
table. Generally, water levels are highest in the spring
and lowest In the late summer or fall.
179. Gilbert, G. K. 1899. Sculpture of the Niagara limestone.
Bulletin Geological Society of America. 10: 122-125.
A discussion of observations and samples taken of the
limestone in the area of Western New York and adjacent
Ontario. The location, formation, distribution, chara-
cteristics and effects of these formations are discussed.
180. Gilbert, G. K. 1907. Rate of recession of Niagara Falls.
U. S. Department Interior, Geological Survey,
Bulletin No. 306. 31 p.
Readings taken in 1827, 1842, 1875, 1886, 1890 and 1905
indicate an average recession for the Horseshoe Falls of
5 ft./year while that of the American Falls is 3 inches/
year. A rather detailed description of survey techniques,
falls features and geographic formation accompanies this
paper.
181. Gillette, Tracy. 1940. Geology of the Clyde and Sodus
Bay quadrangles, New York. New York State Museum
Bulletin No. 320. p. 1-158.
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The Clyde and Sodus quadrangles are located in west
central New York and have Lake Ontario as their northern
boundary with their southern limit approximately one mile
south of the Wayne County line. A detailed stratlgraphic
relationship is given followed by a discussion of the
historical, glacial and economic geology of the two
quadrangles.
182. Gillette, Tracy. 19*17. The Clinton of western and
central New York. New York State Museum Bulletin
No. 341. 191 p.
Except for a limited region in the vicinity of Clinton,
N. Y., where the strata outcrop in the highland to the
south of the Mohawk River, the Clinton underlies the
plains to the south of Lake Ontario and the low areas
surrounding Oneida Lake. Included in the report is a
discussion of the general characteristics of the Clinton
group, detailed stratigraphic and paleontologic relations,
historical geology, description of sections from the
Niagara gorge through Willowvale and a description of
diamond drill cores.
183. Godin, G. 1971. Hydrodynamical studies on the St.
Lawrence River. Canadian Department of Energy,
Mines and Resources, Ottawa. No. 18. 116 p.
Use has been made of the fundamental concepts of hydro-
dynamics to study the steady and tidal flows in the St.
Lawrence River.
The equations of hydrodynamics take on a very simple form
for steady flow as it is the case between Montreal and
Trois Rivers. The definition and the meaning of the
quantities they relate such as the mean depth D, the
inclination of the river bed I, of the surface Sx, have
been carefully reviewed. The mean inclination of the
surface of the river Sx, which is always positive, is
found to be remarkably constant from year to year in
spite of the variations occurring in the discharge.
Using this fact, it is possible to reduce a value of
the Chezy coefficient between Montreal and Sorel.
A plot of the mean level for all the stations located
between King Edward Pier in Montreal and Points au Pere
shows the mean downwards slope of the surface of the
river when undisturbed by the tide. The monthly fluc-
tuations of this mean level decrease downstream since
the capacity of the river bed increases in this direction.
The mean flow is found to be subcritical and, therefore,
cannot impede the propagation of the tide upstream.
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The propagation of the tide may be understood using the
time dependent form of the Equations of Hydrodynamics.
An elementary solution of these equations shows that
under the influence of linearized friction, the tide is
damped exponentially and is retarded in its progress up-
stream. The actual occurrence of quadratic friction in
the equations implies the creation of fast and slow
shallow water constituents along the river; the speed of
progress of the tide uostream is ascertained from observa-
tions. The use of the current observations in conjunction
with the time dependent equations of motion allows the
deduction of the value of the Chezy coefficient which pre-
vails .In the part of the river which extends between
Trois-Riverlers and Quebec.
The spectral analysis of the water levels recorded by the
water level gauges reveals that the low frequency band
contains oscillation of 15, 9, 7 and 5 days which may
be traced to the interaction of the tidal constituents.
The change in phase and amplitude of the major tidal con-
stituents deduced from the same analysis has been plotted
and supplies the material which has to be reproduced in a
mathematical model of the river. The current observations
carried out by G. C. Dohler and the Ship Channel Division
have been analyzed as well, whenever possible. The
suggestion by W. D. Forrester that the average one dimen-
sional currents in a river could be indirectly deduced
from the readings on the tide gauges and the equation of
continuity rather than by direct observations has been
confirmed by our analyses. (Univ. of Toronto, Great Lakes
Institute).
184. Grabau, A. W. 1895. The preglaclal channel of the
Genesee River. Proceedings Boston Society of
Natural History. 26: 359-369.
This paper attempts to show the existence of two northward
flowing preglacial rivers in Western New York, parallel to
the Seneca, Cayuga and other rivers whose valleys are now
occupied by the Finger Lakes. These two rivers are the
Caneseraga and Genesee. Drift deposits forced the Genesee
to leave its ancient course at Portageville and to cut
across the intervening plateau to Mt. Morris, from which
point it occupied the channel of the Caneseraga. Further
glacial action and deposits of materials altered the river
to its present course.
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185. Grabau, A. W. 1901. Guide to the geology and paleon-
tology of Niagara Palls and vicinity. Hew York
State Museum Bulletin No. J4^. 9: 28'J.
A general discussion of geography} geology, stratigraphy
and fossils of the Niagara Palls region, Included is a
bibliography of works completed on the n'clofrv of Niagara
Falls. (Schoellkopf Museum, Niagara Fallen N, Y.>.
186. Great Lakes Basin Hydrolic and Hydro!ogic Data Coordina-
ting Committee. 1958, Lake Ontario outflows.
Committee report. 100 p,
Because of the insignificant amount of watyr contributed
to the St. Lawrence River by sources other than Lake
Ontario, the flow volume of the river is ^n accurate
measure of lake outflow volume. Flow volume vras measured
at these sites: Rapids Flat (Lochs £25,2*0, Gallop Rapids
(Lochs # 27), and long Sault Rapids (Lochs * 23). The
effects of lake and river ice is discussed along with
charts of mean monthly and daily flows,
187. Great Lakes Basic Hydraulic and Hydrologic Data Coordina-
ting Committee. 1962. History of water level
gages, Lake Ontario and the International section of
the St. Lawrence River. Committee report. 163 p,
Location, Operating Agency, data collection, station main-
tenance, history and period of operation from gauging
stations on the shore of Lake Ontario :md thf St. Lawrence
River in the following locations:
Toronto Port Ontario Alcott
Cobourg Qswego Wilson
Brighton Little Sodus Bay Fort Niagara
Kingston Charlotte ' J'ort Wei•or
Tribbetts Point Oak Orchard
Sockets Harbor Sodus Bay
188. Great Lakes Institute. 1964. Data records, '^)62 .
surveys Part I, Lake Ontario and Lake Erie. Great
Lakes Institute, Univ. of Toronto. PR 16,, S'l t>.
Tabulated data for the surface waters of Lake Ontario are
presented on: transparency, temperature., conductivity.
Surface weather observations are also tabulated and they
include: wind direction and speed, visabiJity, 3ky,
cover, opacity, air temperature and dew point, Data on
wave height, direction, period and length are given.
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Descriptive information is also included in the tabula-
tions which give date, time, depth and location of
sampling.
Data obtained during synoptic weather observations is also
tabulated and includes wind speed and direction, mean sea-
level pressure, temperature (air, surface, dewpoint, wet
bulb), cloud amount, type and height, wave direction,
period and height and swell period and height. Solar
radiation data and bathythermograph data are also given.
189. Great Lakes Institute. 1965. Great Lakes Institute data
record - 1963, surveys Part I - Lake Ontario, Lake
Erie and Lake St. Clair. Great Lakes Institute,
Univ. of Toronto. Report PR 23. 193 p.
Data collected by the Great Lakes Institute (on the CCGS
Porte Dauphine) for the year 1963 is summarized in this
report. The Lake Ontario Survey was from stations extend-
ing from Toronto southeast to the center of the lake.
Data was collected on: wind, atmospheric pressure,
humidity, temperature (water and air), clouds, waves,
swells, ladiatlon, water color and turbidity.
190. Great Lakes Institute. 1969. Proceedings - a conference
for the Users of the Great Lakes. Sponsored by the
0-'"r-^io Water Resources Commission, Great Lakes
M.vUute, Univ. of Toronto. 131 p.
A seiies of discussions by representatives of various
governmental agencies to clarify objectives, techniques,
and conclusions. The first discussion session dealt with
water supply and a general debate on related topics.
191. Great Lakes Institute. 1971. Great Lakes Institute data
record-surveys of 1964-Lake Ontario, Lake Erie, Lake
St. Clair, Lake Huron, Georgian Bay and Lake Superior.
Great Lakes Institute, Univ. of Toronto. Report PR
42. 238 p.
Data collected by the Great Lakes Institute (in the CCGS
Porte Dauphine) for the year 1964 is summarized in this
report"! The Lake Ontario survey was from stations extend-
ing throughout the lake. Data was collected on: wind,
atmospheric pressure, humidity, temperature (water and
air), clouds, waves, swells, radiation, water color and
turbidity.
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192. Greeson, P. E., G. W. Williams and P. L. Robison. 1969-
Characteristics of Mew York lakes - Part 1 -
Gazetteer of lakes, ponds and reservoirs. U. 3.
Geological Survey, Albany, New York. Investigation
RI-4. 28 p.
A method is established for computer storage of data on
New York lakes, ponds and reservoirs. Locations of which
are indicated on a map of New York State and general
drainage basin information is presented.
193= Gridwald, R. E. 1951. The ground water resources of
Wayne County, New York. Nextf York State Conservation
Department, Bulletin GW-29. 30 p.
The area of Wayne County comprises two topographic
divisions - a drumlin region and a lake plain. The
climate Is temperate and the mean annual air temperature
is 47°p. The average annual precipitation is 36 inches.
The geology of bedrock and the relationship of properties
and structures of the bedrock to the ground water supply
is discussed.
Grunsky, C. E. - See: R. E. Horton, No. 212.
Gunwaldsen. R. W., B. Brodfield and G. E. Hecker. 1970.
Current and temperature surveys in Lake Ontario for
the James A. Pitzpatrick nuclear power plant. Pro-
ceedings 13th Conference Great Lakes Research.
pp. 914-926.
Measurements of lake currents and temperatures were
made offshore from Nine Mile Point to approximately
seven miles east of Oswego, New York. Two underwater
towers, installed an approximately 7-13 m of water,
were equipped with self contained instruments at various
depths from May to October 1969. Two current pattern
surveys were conducted by releasing approximately 50
drogues which were traced by aerial photography over a
one square mile area adjacent to the shore. Air borne
infrared radiometry was used to measure surface tempera-
tures during the current pattern survey. Current data
indicate the frequency of various speeds, directions and
durations. Temperature records show the gradual seasonal
change, as well as the relatively rapid variations caused
by oscillations in the thermocline.
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195. Hachey, H. B. 1952. Verticle temperature distribution
In the Great Lakes. Fisheries Research Board of
Canada. 9: 325-328.
This paper presents data and conclusions of a study of
thermal distribution in Western Lake Ontario. The thermo-
cline was found as deep as fifty feet and a temperature
change witbin of up to twenty-six degrees Fahrenheit.
The variance of surface layer thickness is also discussed.
196. Haefeli, C. J. 1970. Regional groundwater flow between
Lake Simcoe and Lake Ontario. Department of Energy,
Mines and Resources, Inland Waters Branch. Technical
Bulletin No. 23. 42 p.
The configuration of the water table corresponds generally
with the topography. Prezometric, hydrogeochemical and
mathematical analysis demonstrate the non-existance of
major seepage from Lake Simcoe into Lake Ontario basin.
The groundwater divide coincides approximately with the
basin boundary in the quarternary deposits, as well as in
the different underlying bedrock formations. Geological
and hydrological data are discussed in depth.
197. Hall, J. 18^3- Geology of New York. Survey of the
Fourth Geological District. Carroll and Cook
Printers, Albany, New York. 681 p.
Geological survey of materials and land formations of
Western New York State. Includes descriptions of Lake
Ontario shore processes and elevation of various land
forms. A very detailed description of properties and
structures.
198. Hamblin, P. F. 1968. The variation of the water level
in the western end of Lake Ontario. Proceedings llth
Conference Great Lakes Research, pp. 385-397.
The variation of the water level in the western end of
Lake Ontario is investigated by a number of analyses of
hourly level water data. Water level gauges located at
Toronto, Hamilton, and Port Weller provided data of two
four month periods; one extending from June to September,
the other from December to March. Attention is given to
the detection of the frequencies of the uninodal and
binodal longitudnal surface seiches, to the frequency of
the semidiurnal tide and to the frequencies of the water
level variation associated with disturbances of the
atmospheric wind. In order to examine water level read-
ings for the presence of rotation of the cotldal lines
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about the western end of Lake Ontario. The geometric
configuration of the plane passing through the surface
heights at each of the three gauge stations is computed.
Periodic changes in the orientation of this plane and in
the water level readings themselves are examined by
spectral and cross spectral analysis. Several episodes
of amphidromic motion are detectable. In addition, theory
of free surface oscillation is discussed and some details
of the analysis are described.
199. Hamblin, P. P. 1971. An investigation of horizontal
diffusion in Lake Ontario. Abstract of paper pre-
sented at 14th Conference Great Lakes Research.
pp. 162-163.
Predicting the response of the lakewide water quality to
changing levels of concentration of imputs depend on a
number of biological, chemical and physical processes.
Physical factors of importance are lakewide circulation
and large scale diffusion. Rhodamine B dye was pumped
in a large quantity onto the surface and allowed to
diffuse. After 29 hours the resulting plume covered a
large horizontal area which was analyzed for diffusion
patterns.
200. Hamblin, P. P. and G. K. Rodgers. 196?. The currents
in the Toronto region of Lake Ontario. Great Lakes
Institute, Univ. of Toronto. PP 29. 131* p.
Beginning in June 1966, the Great Lakes Institute embarked
on a programme of observation of water movement, winds and
water temperatures in a region of Lake Ontario adjacent to
Metropolitan Toronto. The programme was undertaken in
pursuance of two scientific objectives: first, the des-
cription of the climate of the current in the Toronto area
and second, to draw conclusions about the behavior of
currents as related to determining variables. Such as
understanding of the relation of currents to the causative
forces would not only be an important advance of the
physical understanding of the Great Lakes but would serve
as a basis for the forecasting of currents in the near-
shore areas. This, in turn, can be useful to those
designing the operating water processing installations.
Initially, various techniques of current measurement used
in the past and present were examined critically with a
view to evaluation of their relative effectiveness in
description of the flow close to shore.
These studies were made possible through the generous
support of the Ontario Water Resources Commission.
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Though advanced studies of the data collected In the field
season of 1966 continue, this presentation is the full
reporting of the observation taken in the field up to
March 31, 196?.
The region of interest extends for some 20 km along the
northern shoreline of Lake Ontario from Humber Bay on the
west to Scarborough Bluffs on the east and offshore for
approximately 5 km. Within this general area, a key
location for the most extensive series of observations
was chosen about 1 km directly offshore from Balmy Beach,
Toronto.
201. Hartnagel, C. A. 1969. Geologic map of the Rochester
and Ontario Beach quadrangles. New York State
Museum. Bulletin II2!. Paleontology 17. 32 p.
The quadrangles are discussed with reference to geology,
geological formation, stratigraphy and erosion. Many of
the beach and shore areas are discussed as to erosion
unusual formations, properties and structures and
occurrences.
202. Hayes, G. E. 1839. Remarks on the geology and topography
of Western New York. American Journal of Science.
25: 87-105.
A general description from observation of the geology and
topography of Western New York. Much data is presented
on the topography and geology of the southern shore of
Lake Ontario. The author describes the shorelines as
consisting of a 5 mile wide band of red sandstone ending
in a large limestone terrace at varying distances from
the lake.
,:03. Heath, R. C. 1964. Ground water in New York. New York
State Conservation Department, Water Resources
Commission. U. S. Geological Survey. Bulletin
GW-51. 1 sheet.
Ground water data for New York State is presented with
data on precipitation, runoff, streams and geology.
A large map of the ground water characteristics is
accompanied by written explanations.
Hecker, G. E. - See: R. W. Gunwaldsen, No.
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204. Herdendorf, C. E. 1970. Lake Erie physical limnology
cruise, midsummer 196?. Report of Investigations
No. 79, State of Ohio Department of Natural Resources
Division of Geological Survey, Columbus. 77 p.
Tabulated data for the surface water of the Niagara River
at Buffalo are presented on: water temperature, current
velocity and direction, conductivity, pH, color and tur-
bidity. The location of the sampling station, time and
date of sampling, and depth of sample are also given.
Surface observations are made which include: wind direc-
tion and velocity and wave direction and height.
205. Heubusch, Carol A. Undated. How the great glaciers
changed the Niagara Frontier. Buffalo Museum of
Science, Hobbies. 38(3): 10.
A general discussion of the topography of the Niagara
frontier before the glacier invasion is given. This is
followed by a discussion of the changes brought about by
the glaciers. Such as the land features formed by
deposition, the origin of the Finger Lakes and the Great
Lakes, the formation of Niagara Falls and the rock parti-
cles making up the glacial drift.
206. Hiney, R. A. 1969. Optimum regulation of the levels of
the Great Lakes. M. S. thesis, State University of
New York at Buffalo. 84 p.
In 1964 the governments of Canada and the United States
authorized a massive international study to determine
what measures could be taken to further regulate the
levels of the Great Lakes. A regulation subcommittee is
currently devising and testing regulation plans in an
endeavor to find one plan that will best serve all Great
Lakes Interests.
This thesis investigates the feasibility of using a
dynamic programming algorithm to find this optimum regu-
lation plan given objective functions relating dollar
losses of each interest to monthly mean lake levels and
outflows. The optimum plan will be that which minimizes
these objective functions for a given set of inflows and
flow constraints.
Inflov; sequences will consist of both the recorded
adjusted net basin supplies and 390 years of artificial
monthly net basin supplies simulated to preserve as
nearly as possible the serial and interlake correlations
observed during the period of record.
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The regulation rules will be derived from a multiple
regression analysis. The resulting empherical formulas
will relate the monthly regulated outflow from each lake
to significant hydrological parameters such as antecedent
Inflows and current lake levels. Comparison of losses
incurred with the derived plan to those which would occur
for the same inflows and existing conditions will indicate
the benefits attributable to the plan.
Hobson, G. D. - See: R. J. Donate, No. 161.
207. Hobson, George D. and J. Terasmae. 1968. Pleistocene
geology of the buried St. David's Gorge, Niagara
Palls, Ontario. Geophysical and Palynological
Studies, llth Conference Great Lakes Research
(Abstract), p. 20.
A startlgraphic drilling project was undertaken in the
1965-66 winter season, following geophysical studies
designed to determine the location, width and depth of
the buried ancient Niagara River Valley leading from
the "whirlpool" of the present river to St. David's
and thence north toward Lake Ontario. Depths belot\r the
surface in excess of 150 ft. have been calculated result-
ing in a channel approximately one mile wide incised
into bedrock to a depth of about 80 ft. Cold climatic
conditions are inferred from the palynological evidence
and a late mid-Wisconsin age has been assigned to the
non glacial beds. The St. David's gorge was cut either
during the last interglacial (Sangamon) interval, or
earlier.
208. Hobson, George D. and J. Terasmae. 1969. Pleistocene
geology of the buried St. David's Gorge, Niagara
Falls, Ontario: Geophysical and Palynological
Studies. Department of Energy, Mines and Resources.
Geological Survey of Canada. Paper 68-67. 16 p.
A stratigraphic drilling project was undertaken in the
1965-66 winter season, following geophysical studies
designed to determine the location, width and depth of
the buried ancient Niagara River valley leading from the
"whirlpool" of the present river to St. Davids and thence
north towards Lake Ontario. J. W. W. Spencer in 1905
delineated a buried channel in the bedrock from the
"whirlpool" to St. Davids.
The geophysical studies consisted of a refraction seismJc
survey utilizing a portable hammer seismograph and
delineated a bedrock depression extending northwestxvard
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from the Whirlpool Rapids to the St. David's Gorge and
northward below the Niagara escarpment to a point east
of Virgil where the channel appears to bifurcate with
one branch extending northward to Lake Ontario and the
other northeasterly to the Niagara River. Depths below
surface in excess of 150 feet have been calculated
resulting in a channel approximately one mile i«?lde
incised into bedrock to a depth of about 80 feet, Sub-
sequent drilling has verified the seismic picture.
No fossillferous beds were found in the boreholes between
St. Davids and Lake Ontario below the Niagara escarpment.
In the St. Davids Gorge, however, borehole 5 revealed the
presence of pollen and plant macrofossils in silt, clay
and sand at a depth of 106-183 feet from surface. These
beds are both overlain and underlain by glacial deposits.
Wood from the 150-foot level was dated at 22,800+450
years before present (GSC-816). Pollen assemblages in
samples taken from the 80-foot sequence of nonglacial
beds were dominated by spruce (P/cea) and pine (P-inuA
ba.nk&J.a.na.) with small numbers of fir (Ab-teA), birch
(Be.tu.ia} and several different types of non-tree pollen
(including f. ex. A^em/c4-ca, Ambloma and C'tenoporf-taceae).
Spores and ferns, fungi and Se.lagj.ne.lia were found in some
samples and pre-Pleistocene spores were present frequently
Moss leaves, fragments of bark, leaf cuticle and conifer
needles, and twigs indicate presence of local vegetation.
Cold climatic conditions are inferred from the palynolo-
gical evidence and a late mid-Wisconsin age has been
assigned to the nonglacial beds. The St. Davids Gorge
was cut either during the last interglacial (Sangamon)
interval, or earlier.
209. Holley, G. W. 187*1. The proximate future of Niagara,
review of Prof. Tyndall's lecture thereon. Proceed-
ings American Association Advancement of Science,
32nd Meeting, pp. 117-163.
A general discussion is presented on the rate of erosion
of Niagara Palls with reference to previous estimates of
falls positions In the future. Many sketches are
reviewed to ascertain erosion rate. The author arrives
at estimates much larger than Professor Tyndall and pre-
dicts the falls will be at the upstream point of Goat
Island before 5000 years at an erosion rate of about
12,000 years/mile.
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210. Holleyman, J. B. 1966. Some results of the program
conducted by Great Lakes - Illinois river basins
project on the Great Lakes. Proceedings 9th Con-
ference Great Lakes Research, Great Lakes Research
Division, Univ. of Michigan. Publication 15. pp.
323-331.
A study of water pollution of the Great Lakes is being
conducted by the Federal Water Pollution Control Admin-
istration. To gain an understanding of the motion of
pollutants in the lakes, networks consisting of instru-
mentation to record lake current and surface wind data
were established in Lakes Michigan, Erie and Ontario.
These networks and instrumentation are described, tabu-
lations of available data are presented and the collection
and reduction of data are briefly discussed.
Winds recorded by the network and winds observed aboard
ships navigating the Great Lakes are compared with geo-
strophic winds determined from synoptic weather maps.
The results are presented in terms of ratios of actual
wind, speeds to geostropic wind speeds and deviation in
direction of actual winds from the direction of geostro-
phlc winds.
Holroyd, E. W. - See: J. E. Jiusto, No. 223.
Horton, A. H. - See: H. K. Barrows, No. 26.
2il. Horton, J. H. 1968. Shorecliff erosion on the north
shore of Lake Ontario at Scarborough, Ontario.
llth Conference Great Lakes Research (Abstract).
PP- 7^-75.
Field studies of erosional processes acting on complex
unconsolidated glacial and interglacial shorecllff
materials were carried out at Scarborough on the north
shore of Lake Ontario during the period of November,
1965 to October, 1966. Precise photogrammetric mapping
of the Shorecliff topography was carried out for five
sample reaches of shoreline, each with a different
stratigraphlc sequence. Comparative mapping for each
sample was compiled from 1931, 1952 and 1964 aerial
photography.
212. Horton, R. E. and C. E. Grunsky. 1927. Hydrology of
the Great Lakes. Report of the Engineering Board
of Review. Part 3, Appendix 2. Chicago, Illinois.
432 p.
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Hydrology has to do with the occurrence and distribution
of natural water resources and with their quantitative
variations resulting from the operation of the hydrologic
cycle—rainfall, runoff and evaporation. As related to
the Great Lakes it involves the following elements:
1. Rainfall on the drainage basins tributary to the
lakes.
2. Rainfall on the lake surface.
3. Evaporation from the lake surfaces.
4. Runoff and inflow to the lakes.
5. Outflow from the lakes.
6. Lake levels and their fluctuations.
Among the earliest measurements of outflow from the
Great Lakes are those made under the direction of Col. J.
Kearney of the U. S. Topographic Engineers, in October,
1856. He found the combined flow through the north,
middle and south passes of the St. Clair River through
St. Glair Flats, to be 212,000 cubic feet per second.
Much more extensive measurements were made by D. Parrand
Henry in 1865-69. Henry also made measurements of the
evaporation at stations surrounding the lakes and under-
took to determine the relation between runoff, inflox-/,
rainfall, evaporation and outflow for Lakes Michigan and
Huron. Beginning about 1896, numerous and reliable
gaglngs of outflow from the different lakes have been
made under the direction of the U. S. Lake Survey.
Complete records of lake levels extend back to i860 and
approximate records can be carried back to 1835• Exten-
sive data of rainfall on the Great Lakes drainage basin
have been maintained in the United States by the U. S.
Weather Bureau, the longer records extending back to the
beginning of lake level records. Similar records in
Canada have been maintained by the Canadian Meteorological
Service. Pew data regarding runoff to the lakes from
tributary streams are available prior to 1900.
Several attempts have been made to correlate the stage
and discharge relations of the Great Lakes with the
controlling factors—rainfall, evaporation and runoff.
In general, it has not been possible heretofore to obtain
satisfactory results from comparisons of inflow and out-
flow for want of some of the essential basic data,
particularly records of runoff from tributary streams.
Attention is attarcted to this subject at the present
time through a variety of causes:
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1. The increasing importance of navigation of the
Great Lakes.
2. The agitation for waterways connecting the Great
Lakes with the Atlantic Ocean and the Gulf of Mexico.
3. The present low stages of the lakes.
4. The obvious need of lake level regulation, whether
any water is diverted from the Great Lakes or not.
While higher minimum stages of the lakes are desirable,
higher maximum stages may be undesirable. In general,
a decrease in the range of fluctuation of lake levels
through operation of regulating works must be accompanied
by an increase in variation in discharge or vice versa.
The problem of regulation is to maintain the highest
practical minimum stages during the navigation season
and the most desirable regimen of outflow compatable
therewith without introducing; objectionably high maxi-
mum stages or outflow velocities. The solution of this
problem depends in a large measure on the range and
magnitude of different types of variation in lake levels
particularly variations due to natural secular variations
of rainfall on the runoff from the lake drainage basins.
Changes or variations in lake levels are due to a variety
of causes, which may be classified as natural or artifi-
cial. Variations due to natural causes include those
resulting from variations in rainfall and evaporation,
those due to ice conditions and erosion and transient
variations due to barometric changes, wind action,
seiches, currents, tides and waves. Artificial changes
include those resulting from channel improvement, con-
trol works and diversions.
Variations in lake levels may also be conveniently
classified according to their duration.
(a) Permanent
(b) Secular
(c) Seasonal
(d) Transient
Permanant changes may have resulted from tilting of the
lake basins, erosion and artificial improvement of
connecting channels, and from diversions. Secular
changes are those of long duration, due principally to
variations in rainfall and evaporation. Seasonal
changes are due to the natural annual cycle of rainfall,
runoff and evaporation and to the effect of ice condi-
tions. Transient changes include those due to wind
barometric variations, seiches, tides, currents and
waves end in some c?..ces, Ice .jams.
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One of the objects of the study of the hydrology of the
Great Lakes is to provide a basis for the more accurate
evaluation of the effects of some of the more important
causes of changes in lake levels. These include parti-
cularly the varying effects of rainfall, evaporation
and ice conditions and the effect of improvement of the
connecting channels between the lakes.
Aside from the secular changes in natural conditions,
such as variations in annual rainfall, runoff and evapora-
tion, there have been important geographic changes in the
Lakes region in recent times. These include:
1. Deformation or tilting of the land surface, to which
attention was directed by Dr. G. K. Gilbert many years
ago.
2. Deformation and changes in agricultural conditions,
particularly the possible effect of the cutting off
of the primeval pine forest of northern Michigan.
3. Deepening arid improvement of the lake outlets at
control points, particularly on St. Clair and Detroit
Rivers.
4. Artificial diversions from the lakes.
Some of these changes, such as channel improvement and
diversions, are known to have affected the hydrology of
the Great Lakes, and their effects can be quantitatively
determined within certain limits of approximation.
While it may not be possible at the present time to
determine with precision the effects of tilting and
deforestation in relation to the hydrology of the Lakes,
yet a discussion of this subject may serve to clarify
the situation by showing at least the relative importance,
or lack of importance, of these factors as compared with
other factors affecting lake levels and outflow.
213. Hough, J. L. 1958. Geology of the Great Lakes. Univ.
of Illinois Press, Urbana, Illinois. 313 p.
A very comprehensive book about Lake Ontario Including
the following parameters:
General Description Sediments
Depth Lake Stages
Bottom Topography Extensive Bibliography
Geology Seiches & Short Period
Wave Action Fluctuations
Tides Ice
Surface Currents Thermal Stratification
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Precipitation Pre Glacial & Glacial History
Evaporation Maps
Chemistry
214. Hough, J. L. 1963. The prehistoric Great Lakes of
North America. American Scientist. 51: 84-109.
The origin and evolution of the Great Lakes basins are
discussed in depth in this article. The various lake
stage-glacial retreat stages are depicted along with an
explanation of basin flow characteristics and changes
in them. The Great Lakes Basin originated presumably
from large pre-glacial rivers in the area that were
altered by the glaciers.
A discussion of post glacial activity is also presented
showing the development of water systems and lake levels
as we know them today.
215. Hyde, A. S. 1939. The ecology and economics of birds
along the northern boundary of New York State.
Roosevelt Wildlife Bulletin. 7(2): 66-215.
Basic Information are presented on the geology and
climatology of the northern boundary of New York State,
much of which is along the St. Lawrence River and Lake
Ontario. Mean summer monthly and annual precipitation
temperatures and humidity are presented.
216. Hydro-Electric Power Commission of Ontario. 1965. Brief
to International Joint Commission on Great Lakes
levels. Toronto. 9 p. + graphs.
It is also felt that regulation could be a benefit to
all users provided all lakes are regulated to a coordina-
ted plan and that such a plan gives equitable considera-
tion to the requirements of all users. Ontario Hydro,
and therefore, Ontario, has large investments in hydro-
electric plants on the lakes. As regulation could have a
considerable effect on the output of these plants, it is
respectfully requested that an opportunity be given this
Commission to comment and advise on criteria on which the
regulation studies will be based and on any proposed
regulation plan while it is in the formative stages.
(Univ. of Toronto, Great Lakes Institute).
217. International Joint Commission. 1951. Pollution of
boundary Waters. Washington, D. C. 311 p.
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This report, published by the International Joint
Commission, presents data on Eastern Lake Erie, the
Niagara River and Western Lake Ontario. The following
parameters are presented: temperature, precipitation,
average annual wind direction and velocity, and water
turbidity. Practical Information is also presented on
the industrial and domestic uses of these waters and
their biological, chemical and physical effects on the
water quality of the area.
218. International Joint Commission. 1968. Interim report
on the regulation of Great Lakes levels. Washing-
ton, D. C. 21 p.
A Joint Canada-United States study on the water levels
of the Great Lakes has been undertaken in response to a
reference, dated October 7, 1964, to the International
Joint Commission by the Governments of the two countries.
The reference, a copy of which is appended hereto,
requires a determination of whether measures within the
Great Lakes Basin can be taken in the public Interest to
further regulate the levels of the Great Lakes or any of
them and their connecting waters, so as to reduce the
extremes of stage which have been experienced.
This interim report describes features of the lakes
which relate to their levels; Indicates the interests
which make direct use of the lakes and are affected by
lake level variations; discusses the problem of regula-
ting the levels by controlling lake outflows; sets forth
the nature, scope and progress to date of the Commissions
study and Indicates how it is oriented toward a compre-
hensive consideration, within the terms of reference of
the many facets of the lake-regulation problem.
219. International Joint Commision, 1969. Pollution of Lake
Erie, Lake Ontario and the International Section of
the St. Lawrence River. Washington, D. C. 3: 329.
The intensification of the pressures responsible for
water pollution in the Lake Ontario basin are described.
The projections of population growth and industrial
developments indicate a probable doubling by 1986 of the
raw waste loadings produced by municipalities and Indus-
tries. Lane drainage has been cited as causing signifi-
cant pollution problems but practical control measures
are not yet readily available. Waste heat and losses of
oil and industrial materials are not new problems,
however, their magnitude has grown. It is clear that
future requirements for cooling water and the discharge
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of large quantities of waste heat will pose serious
questions on how to protect or preserve the ecological
environments of nearshore waters. Industrial growth and
increasing vessel traffic in the Great Lakes will create
further potential hazards for spills of oil and hazardous
materials unless precautions are taken to prevent such
occurrences. Improvement in the quality of the water can
be expected with phosphorus reduction in the drainage
basin provided that the recommended implementation
programs are developed and carried through by municipal-
ities and industry.
220. International Joint Commission. 1970. Pollution of
Lake Erie, Lake Ontario and the International Section
of the St. Lawrence River. Washington, D. C. 4: 1?4,
In depth discussion on biological and chemical parameters,
with some basic information on drainage, sedimentation and
water turbidity.
221. International Joint Commission. 1971. The Niagara River
pollution abatement progress. Lake Erie, Lake
Ontario Advisory Board. Washington, D. C. 62 p.
Although the Canadian side of the Niagara River is
relatively pollution free, discolorization and oil pollu-
tion problems are still present near some outflows on the
American side of the river. Industrial and domestic
effluents are traced. Each of the major contaminants of
the river are discussed, along with the effects on general
river water quality.
Irbe, J. G. - See: T. L. Richards, No. 315.
222. Irbe, J. G. 1969. Some unusual surface water tempera-
ture patterns in the Great Lakes, as detected by
airborne radiation thermometer surveys. Proceedings
12th Conference Great Lakes Research, pp. 583-607.
Since 1966, the meteorological service of Canada has
undertaken a program of monthly surface water temperature
surveys of the Great Lakes bordering on Canada using an
airborne infra-red temperature sensing device. During
the three year period that the program has been in pro-
gress, many interesting features of the distribution of
surface water temperature have been found. Maps showing
some of the more unusual isotherm patterns deduced from
these surveys are presented and discussed with reference
to lake circulation and meteorological conditions.
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Isachsen, Y. W. - See: J. G. Broughton, No. 39.
Isachsen, Y. W. - See: D. W. Fisher, No. 172.
Izatt, J. B. - See: M. D. Palmer, No. 293-
Jekel, P. - See: J. T. Scott, No. 3^3.
223. Jiusto, James E. and E. W. Holroyd. 1970. Great Lakes
snowstorms, Part I. - cloud physic aspects. Abstract
of paper presented at the State University of New
York, Atmospheric Sciences Research Center, Albany,
New York. p. 10.
Lightning discharges observed in Great Lakes snowstorms
during early winter can be explained by heavy riming of
crystals. Based on field observations and calculations,
the following criteria appear essential for the
phenomenon:
(a) Supercooled clouds with a large water-to-ice
ratio (clouds close to water saturation).
(b) The presence of large graupel pellets (conical
shapes appear particularly favourable for charge
separation).
(c) Cloud thickness of at least 3-4 km.
(d) Relatively extensive cloud cells (radar echoes
with 10 km or more horizontal dimensions).
In essence, items (a) and (c) provide for the effective
growth of graupel to large sizes, and item (d) enables a
sufficient volume of cloud togenerate a total critical
charge of about 1000 C (Mason, 1962). The above condi-
tions are satisfied during the early winter season—
November and December—when in fact lightening is observed.
As reported in the snowfall climatology discussion, these
intense storms produce 2 to 5 times more snowfall than late
winter storms.
224. Jiusto, James E. and M. L. Kaplan. 1970. Snowfall
characteristics of Great Lakes storms. Abstract of
paper Proceedings 27th Annual Meeting Eastern Snow
Conference, Albany, New York (February, 1970).
Snowfall data downwind of Lakes Erie and Ontario were
analyzed for 26 individual "lake effect" storms during
the three-year period 1966-68. This beginning clima-
tology included arial distributions of total snoivfalls,
snowfall depth to meltwater ratios and total meltwater
values. A statistical analysis was performed to explore
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the influence of cloud microphysical, seasonal (tempera-
ture), and topographic factors on these snowfall
characteristics. Relationships were also sought between
upper-air flow patterns and total volumetric water output
per storm. (Canada Centre for Inland Waters).
225. Jiusto, James E., D. A. Paine and M. L. Kaplan. 1970.
Great Lakes snowstorms, Part 2. Synoptic and
cllmatological aspects. Abstract of a paper pre-
sented at Atmospheric Sciences Research Center,
State University of New York, Albany. 58 p.
A climatologlcal study of three years of lake-storm pre-
cipitation data served to solidify certain previously held
ideas on storm behaviour and to Introduce some new find-
ings. Snowfall distributions in the vicinity of Lake Erie
and Lake Ontario are indeed dependent on air trajectory,
with the greatest snowfall amounts being associated with
southwest to westerly winds and a single intense snow-
band. Each of these intense storms generates an average
of approximately 3 x 10 Ibs. of water and a snowfall
area of approximately 50,000 nautical mi (both lake
regions combined). Storms associated with northwesterly
winds, consisting of multiple less-intense bands, produce
dome 50$ less total precipitation on average, with the
snowfall spread over a somewhat greater area. Orographic
effects, while a factor in snowfall accumulations,
generally appear less Important than lake-induced and
synoptic-scale (vortlcity advection) Influences.
Snow crystal type, as deduced from snowfall density (snow
depth to meltwater ratio), is highly variable within a
given storm as well as from storm to storm. The data
Indicate that rimed crystals and graupel are common close
to the Lakes during November and early December, while
snowflakes (aggregates) become the dominant crystal type
further inland. As the winter season progresses and lake
and air temperatures decrease, rimed crystal forms become
far less common. These results are compatible with sparse
field observations.
Water budget analyses show a strong correlation between
amount of snowfall and time of year, with January storms
being 2 to 5 times less productive than early-season
snows. A steady decline in lake temperature and in air-
water temperature difference are largely responsible and
obviously result in reduced vertical fluxes of moisture
and thermal energy. Perhaps no better sample of the
impace of these water bodies on Great Lakes snowstorms
can be given. (Canada Centre for Inland Waters).
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226. Johnson, E. C. and C. P. Moon. 1953. The heavy snowfall
of January 28-30th, 1953, at the eastern end of Lake
Ontario. Monthly Weather Review. 8l(l): 26-30.
On January 28 and 29, 1953, three feet of snow fell in a
20 mile wide east west band centering around Polaksi, New
York. The following situations were thought to be
responsible:
1. Polar air over Lake Ontario on January 28 brought
snow to Polaski.
2. An east-north-east shift on the 29th centered the
storm around Adams, New York with an accompanying 9"
of snowfall.
3. A shift back toward Polaski gave the area another 2"
of snow.
4. A final shift to the east-south-east on the 29th and
30th brought 1 foot of snow to the area of Fulton and
Syracuse.
5. The temperature difference between air and Lake
Ontario water was alv?ays greater than 10°F.
The snow was of light density causing severe blowing and
drifting.
227. Johnston, R. H. 1964, Ground water in the Niagara Falls
area, New York. U. S. Geological Survey, New York
State Conservation Department. Water Resources
Commission, Bulletin GW-53. Unnumbered.
Glacial deposits in the Niagara Falls area consist of
(1) glacial till, (2) lake deposits, (3) a few small sand
and gravel deposits. The bedrock is Lockport Dolomite
and Queenston Shale. The Lockport Dolomite is the only
important aquifer. The water is found in verticle and
horizontal joints In the rocks, as well as small cavities
from which gypsum has been dissolved. There are seven
distinct water bearing zones in the area. (Schoellkopf
Museum, Niagara Falls, New York).
Jurkovec, A. A. - See: A. S. Menon, No. 269.
Kamitakahara, G. K. - See: W. G. Simpson, No. 350.
Kammerer, J. C. - See: B. K. Gilbert, No. 178.
Kaplan, M. L. - See: J. E. Jiusto, No. 22*1, 225.
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228. Karrow, P., J. R. Clark and J. Terasmae. 1961. The
age of Lake Iroquois and Lake Ontario. Journal
of Geology. 69: 659-667.
Recent geological and engineering investigations at
Hamilton, Ontario have resulted in the discovery of
buried plant bearing beds in deposits of Lake Iroquois
and Lake Ontario. Fossils in these beds indicate cold,
shallow water conditions of sedimentation for the earlier
deposited beds and warmer conditions for later deposited
layers. Radiocarbon dating of buried wood suggests that
Lake Iroquois was formed during the retreat of Port Huron
ice. The Valders drift boundry is inferred to be north
of Lake Ontario. Lake Ontario probably originated over
10,000 years ago.
Kemp, A. L. W. - See: R. L. Thomas, No. 389.
229. Kemp, A. L. W. 1969. Organic matter in the sediments of
Lakes Erie and Ontario. Proceedings 12th Conference
Great Lakes Research, pp. 237-249.
Six piston core samples were taken in Lake Ontario. The
basin sediments consisted of black laminated grey silty
clay, with mud thicknesses ranging from 4.6-13.8 m In the
cores. A diagramatlc profile Is presented in the paper.
230. Kemp, A. L. W. 1971. Organic carbon and nitrogen in the
surface sediments of Lake Ontario, Erie and Huron.
Journal of Sedimentary Petrology. 41(2): 537-548.
Analysis of 355 surface sediment samples (top cm) from
Lake Ontario, Erie and Huron. Similar analysis were
carried out in a representative core from each lake at
close intervals down to 20 cm. Sediment texture, proper-
ties and materials are discussed.
231. Kemp, A. L. W. and C. P. M. Lewis. 1968. A preliminary
Investigation of chlorophyll degregation products
in the sediments of Lakes Erie and Ontario. Pro-
ceedings llth Conference Great Lakes Research.
pp. 206-229.
Studies of thirty seven surface sediment samples. Sub
environments within the lake are recognized on the basis
of bathymetry, sediment particle size distribution, clay
mineral content and mud thickness.
Kennedy, R. J. - See: A. Brebner, No. 38.
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232. Kilgour, W. J. 1963. Lower Clinton (Silurian)
relationships in western New York and Ontario.
Bulletin of the Geological Society of America.
74: 1127-1142.
A new interpretation of Silurian Lower Clinton relation-
ships observed in the area between Medina, New York, and
Clappison's Corners, Ontario, is presented. The Lower
Clinton Group in this area is considered to include those
units between the Thorold Sandstone and the Irondequoit
Limestone. The profound lithological and faunal differ-
ences between the Lower Clinton strata of western New
York and those of the Niagara Peninsula in Ontario are
probably the result of deposition in a shallow basin
under conditions controlled by proximity to the Cataract
shelf (Bolton, 1957). The influence of this shelf
extended south and east of Hamilton, Ontario; its effect
was felt at the beginning of Early Clinton time. Fre-
quent slight changes in the elevation of the shelf area
and the nearby depositional basin to the south and east
resulted in fluctuations in strand lines and reworking
and removal of some units. Supporting evidence includes
thin conglomerates at several contacts, wedging out or
overlap of lithologic units and changes in fauna of
successive units.
The Reynales Formation between Medina, New York and
Clappison's Corner, Ontario, is restricted and redefined
to include only the lower, fossiliferous, limestone units
which are here designated the Hickory Corners Limestone
Member (new name) and the Merritton Limestone Member
(new name). The upper more dolomltic and less fossili-
ferous unit, herein named the Rockway Dolomite Member
(new name), is removed from the Reynales and is consid-
ered to be the lower member of the Upper Clinton
Irondequoit Limestone.
Kilpatrick, T. B. - See: D. C. Archibald, No. 17, 18,
19, 20, 21, 22.
233- Kindle, E. M. 1915a. Limestone solution on the bottom
of Lake Ontario. American Journal of Science.
39: 651-656.
Pitted limestone rocks found at a depth of 150-200 ft.
southwest of Brighton, Ontario indicate a lack of deposit
on bottom and strong scouring action on the limestone by
deep currents. Sixteen miles of Presque Isle.
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34. Kindle, E. M. 1915b . Notes on bottom currents in Lake
Ontario. American Journal of Science. 39: 192-196.
Using ripple mark molds underwater, a wind direction
current direction correlation is derived for the Toronto
area of Lake Ontario.
Wind Current
north/northwest variable
northeast /east /southeast southwest
south/southwest/west northwesterly
Preaque Isle and Wellington Bay had currents in the
westerly direction at approximately 4 1/2 miles per hour.
'jo, Kindle, E. M. 1925. The bottom deposits of Lake Ontario,
Transactions Royal Society of Canada, 3d Series.
47-102.
The material covered includes , general lake features
(Phisiographic features, water temperature, materials of
the lake shore and its recession), distribution factors
such as wind and currents, physical bottom features
(sedimentation, depth and distance factors on sedimen-
tation, sediment analysis), and organic bottom features
which includes some data in light penetration (by visual
analysis) .
236. Kindle, E. M. A comparative study of different types of
thermal stratification in lakes and their influence
on the formation of marl. Journal of Geology.
37(2): 150-157.
The results of an Investigation of thermal stratification
in Lakes Ontario and Huron are compared with the thermal
stratification x^hich characterizes small lakes in the
Ottawa Valley. The warm surface zones of the Great Lakes
is much thicker than those of the smaller lakes. The
relatively low temperature of the Great Lakes epilimnion
zones prevents marl bed formations,
237. Kindle, E. M. and P. B. Taylor. 1913. Geologic atlas
of the U. S. - Niagara folio. Department of
Interior, Geological Survey. 38 p.
The geology, age determinations, stratigraphy, locations,
dimensions and evolution of the Niagara Polio area of
Western New York. The area covered Includes much of
Niagara Palls, the lower Niagara River., Lake Ontario
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(Niagara Delta area) and shore areas east of the Niagara
River Delta. (Schoellkopf Museum, Niagara Falls, N. Y.).
238. Kirchgatter, D. 1958. Factors responsible for the
recession of the Scarborough Bluffs shoreline,
Canadian Department of Lands and Forests. 24 p,
The total area has been traversed by foot as the base of
the cliffs and to the greater part by car and by foot
along the summit. Contrary to frequently expressed
opinions it was found that in no case waves, or better
breakers were the responsible factors of erosion. This
is within the limitation that we presently experience a
comparatively low lake level. The main factors we con-
sider today are surface water runoff, water seeping out
on the face of the cliff, wind erosion in parts, gullying
and possibly the nesting of cliff swallows and the advent
of the building of houses and roads, etc., close to shore-
line. The answer to counteract erosion might be in
maintaining low water levels, artifically sloping off
pronounced steep cliffs, providing drainage for them., and
to keep any man-made construction well distanced from the
edge of the cliff.
239. Kirshner, L. D. 1968. Effects of diversions on the
Great Lakes. U. S. Army Corps of Engineers, Lake
Survey Report 68-7. 33 P«
Effects of diversions on the levels and outflows of
Lakes connected by channels affected by backwater, such
as Lakes Michigan, Huron and Erie in the Great Lakes
system, are discussed. The diversions considered consist
of diversions into and out of the drainage basin of the
lakes and of diversions between the lakes. The histories
and features of the five existing diversions in the Great
Lakes basin that meet these conditions are outlined. It
is pointed out that the full effects of such diversions
are not immediate upon initiation of the diversion but
are progressive over a period of time, depending upon
the surface areas and the lake level-lake outflow
relationships of the lakes involved. This period is, for
example, about 15 years for Lake Michigan and Lake Huron
diversions. The methods used by the U. S. Lake Survey to
determine the progressive and ultimate effects of diver-
sions in connection with studies of the International
Joint Commission of the United States and Canada are
described. The equations employed and the results in
graphical form are shown. The ultimate effects of the
Great Lakes diversions upon their levels and outflow,,
which have already been reached, are listed. General
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commentary Is made upon the effects of high and low lake
levels and outflows In the three major Great Lakes
Interests ~ rlporian properties, navigation and hydro-
electric power - that are concerned with the levels and
outflows and upon the manner in which increases and
decreases in lake levels and outflows resulting from
diversions increase or decrease the effect. (Canada
Centre for Inland Waters).
2'iO. Klwanas Club of Stamford, Ontario. 196?. Niagara Falls,
Canada, Centennial Volume, Niagara Palls, Ontario.
^52 p.
A history of human development of the Ontario side of
the Niagara River. Included is some material on geology,
river characteristic and evolution. (Schoellkopf Museum,
Niagara Palls,, New York).
2'41. Kramer, J. R. 1966. Equilibrium models and composition
of the Great Lakes. Equilibrium concepts in natural
water systems. American Chemical Society, Washing-
ton, D. C. pp. 243-254.
To a ^ood first approximation, the Great Lakes fit a
model involving the equilibrium of calcite, dolomite,
apatite, Kaolinlte, gibbsite, Na and K Feldspars at 5°C,
1 atmosphere total pressure with air of Pco- - 3-5 x 10-4
atmospheres and water. Dynamic models, considering car-
bon dioxide pressure and temperature as variables, show
that cold waters contain excess carbon dioxide and are
unsaturated with respect to calcite, dolomite and
aputite, whereas warm waters are nearly at equilibrium
i/ith the atmosphere but somewhat supersaturated with
respect to calcite, dolomite and apatite.
Jl° Ku, L. F, 1970. Spectra of monthly mean water level In
the Great Lakes. Proceedings 13th Conference Great
Lakes Research, pp. 844-861.
The- annual variation sa and its harmonics appear signi-
ficant l.v in the spectra of monthly mean water level In
the Great Lakes. The energy of the spectra is concen-
trated in low frequencies and the plots of background
In the spectra at all stations are similar. The coherent
energy between Lake Superior and each of the other lakes
Is relatively lower than that of other pairs. The phase
sa Increases fron east to west. In Lake Superior it lags
about two months behind Lake Ontario. The amplitude of
sa computed by least squares decreases as the number of
points increases. The value of sa in Lake Ontario is
12 cm. larger than that of Lake Huron (6 cm). Owing to
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the relatively small contribution to the variance by
the annual term and. its harmonics, it Is not practicle
to predict the monthly mean water level using only the
periodic components.
Lambert, Y. T. - See: D. V. Anderson, No. 12.
Landsberg, D. R. - See: J. T, Scott, Mo. 3^-
243. Landsberg, D. R. , J. T. Scott and M. Fenlon. 1970.
Summer circulation patterns near Nine Mile Point,
Lake Ontario, Proceedings 13th Conference Great
Lakes Research, pp. 444-452.
Measurement of current speed and direction by current
meter and drogues were obtained in July and August 1969
on three buoy lines located near East Nine Mile Point
on the south shore of Lake Ontario. Transport was found
to be northeastward forming a coastal current with speeds
from 5-40 cm/sec. The speed of this current decreased
rapidly below the thermocline. The coastal current was
weaker near Nine Mile Point than 10-30 km. west because
this current turns northward near Oswego. The dynamic
height pattern shows a countercurrent forming as eddy
west of Nine Mile Point.
Lane, R. K. - See: N. J. Campbell, No. 50.
Lane, R. K. - See: P. C. Elder, No. 165.
244. Lane, R. K. 1970. Great Lakes thermal studies using
Infrared imagery. Limnology and Oceanography.
15(2): 296-300.
Examples of mosaics of infrared imagery of the western
end of Lake Ontario are used to demonstrate their value
in revealing detailed surface thermal patterns. Addi-
tional data from airborne thermometry and shipboard
measurements confirm the interpretation of large-scale
dynamic processes. Smaller scale phenomena, such as
internal wave patterns and small eddies, are also inter-
pretable. (Canada Centre for Inland Waters).
245. Langbein, W. B. , et. al. 1947. Major winter and non-
winter floods in selected basins in New York and
Pennsylvania. 0. S. Geological Survey Water Supply
Paper 915. 139 p.
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The scientific design of flood control works are based on
an evaluation of the hydrologlc factors basic to flood
events, among which are snowfall, rainfall, soil condi-
tions arid channel influences. Precipitation, temperature,
geology, climatology and stream characteristics are
studied for 8 basins in Pennsylvania and New York.
2 '46. Langford, G. 3, 1952. Report on lakeshore erosion -
Fart I - Lake Ontario from Niagara to Cobourg.
Department of Planning, and Development, Province of
Ontario, Toronto., Ontario. 36 p.
Periods of high water accelerate the process of shore
erosion, emphasizing the destructive capacity of waves.
Two high water stages have been reported; one in 1929-30,
the other in 19^3-48, Governmental awareness, legisla-
tion, engineering studies for protective measures and
lake current studies should be initiated to combat the
problem. Recession rates, geological formations and
Materials, and water level data are presented for all the
major geological areas within the shoreline area from
Niagara to Cobourg. (Canada Centre for Inland Waters).
Lansing, L. -- See: J. T. Scott, No. 3^5.
24?. Lansing, L, 1965. Air mass modification by Lake
Ontario during the April-November period. Great
Lakes Research Division, Univ. of Michigan Publi-
cation 13. pp. 257-261.
This paper discusses the important role the Great Lakes
play on the weather and the climate modifications of the
surrounding air masses, by means of a study of the north-
eastern region of Lake Ontario. The study describes the
changing patterns of air mass modifications as the season
progresses through spring, the heat of mid-summer to late
fall, which ice begins to form in the harbors of the lake.
It is indicated that the lake plays a more important role
on the modification of air masses in the fall and early
winter,
248. Laverett, P. 1902. Glacial formations and drawings
features of the Erie and Ohio basins. U,. S.
Geological Survey, Monogram 4l. 802 p.
This survey covers the southern shore area of Lake
Ontario from the Niagara to the Genesee Rivers. Special
emphasis is on drainage system features in the area
(direction, volume, variation). A brief history is
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given of glacial movement and lake formation and an
extensive geological bibliography is presented. Data
is presented on age and composition of geological
formations.
2^9. Laverett, P. and P. B, Taylor. 1915. The Pleistocene
of Indiana and Michigan and the history of the
Great Lakes. U. S. Geological Survey, Washington,
D. C. 529 p.
This report is a lengthy statement of the glacial lakes
and processes occurring in the Great Lakes region result-
ing in the formation of the lakes as we know them today.
The discussion includes, ice characteristics, erosion,
changes in topography, geology, glacial deposits and lake
levels.
Lee, A. H. - See: G. K. Rodgers, No. 330.
250. Lemire, P. 1961. Winds on the Great Lakes. Great Lakes
Institute, Univ. of Toronto. PR-2. 11 p.
This project was carried out with two main objectives in
mind. The first was to calculate the ratio of the winds
over water to those over land. The second was to compare
the actual observed wind velocities with those calculated
from surface weather maps.
The results of the first analysis of winds over water and
over land showed that there is a good relationship and
that this relationship displays two strong variations -
diurnal and seasonal. The ratio R varies during the day
from a maximum at approximately 00 E.S.T. to a minimum
at 13-14 E.S.T. This ratio R also displays a seasonal
variation from a maximum during December-January to a
minimum during July-August. After comparing all results
obtained, we find that regardless of the lake chosen, the
average values for the ratios were:
R fall =1.9 and R spring =1.6
In regard to the relationship between the observed winds
and those calculated from the surface weather maps, we
have also found a good correlation. This ratio has only
one discernible variation - it varies Inversely as the
magnitude of the observed wind and this relationship is
approximately linear. The average value of the ratio R,
(where R, = geostrophic wind speed/observed wind speed)
was founa to be approximately 1.4. That is to say, for
a case of indifferent stability the geostrophic wind
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calculation would likely be greater than the observed
winds by a factor of I.1*. This result seems to be fairly
consistent with the generally accepted ratio of three
halves (5, 8).
Lewis, C. P. M. - See: A. L. W. Kemp, No. 231.
Lewis, C. P. M. - See: R. L. Thomas, No. 389.
251. Lewis, C. P. M. and R. N. McNeely. 196?. Survey of Lake
Ontario bottom deposits. Proceedings 10th Conference
Great Lakes Research, pp. 133-142.
Short gravity cores and grab samples recovered during a
continuing reconnaissance survey initiated in 1966, were
used to study the distribution, stratigraphy and chrono-
logy of Lake Ontario bottom deposits. Three major groups
of surficial deposits were recognized: 1) complex near-
shore sediment, 2) glaciolacustrine clays, 3) post
glacial muds. Organic content of 2-6% and median
particle diameters of 1-4 microns are typical of the
offshore surficial muds. Pollen in these sediments
facilitates correlation and subdivision and indicates
that the present sedimentation rate in the main basin is
approximately 10 cm per century. Several sediment
sequences indicate and confirm the post glacial low level,
Admirality Lake stage and suggests it may have reached
lov^er levels than previously believed.
252. Lewis, C. P. M. 1968. Quaternary geology of the Great
Lakes. Geological Survey of Canada, Paper 68-1.
Report of activities, Part A: April-October.
pp. 63-64.
A major coring and echo sounding program in Lake Ontario
yielded piston cores up to 60 feet in length from rep-
resentative areas of mud throughout the lake. The
departmental vessel C.S.S. Limnos proved to be an ideal
platform for these operations. A variety of shallow
water environments were Indicated.
253. Lewis, C. F. M. 1971. Stratigraphy and sedimentation
from seismic profiling in the Toronto waterfront
area of Lake Ontario. Abstract of paper presented
at 14th Conference Great Lakes Research, Toronto,
April 19-21, 1971. PP. 168-169.
Between Humber Bay and Scarborough, the lake bottom
shelves gently offshore into depths of 9 to 23 m. This
shelf is veneered with sand and/or gravel, and glacial
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sediments locally outcrop. Bar forming processes may be
active on the shallow shelf and nrofiles indicate an
irregular bottom topography. A pronounced break in slope
terminated the shelf in the form of a bold scarp feature.
Bedrock outcrops on the shoreline at Minico, elsewhere in
the Toronto area it lies 6-30 m below the lake level, and
slopes gently offshore at a slightly greater rate.
Lewis, J. M. 1963. The present state of knowledge of
the Great Lakes current system. M. S. Dissertation,
Univ. of Chicago, Chicago, Illinois. 50 p.
An attempt has been made to summarize the work that has
been done on the Great Lakes current system. The summary
includes the technological aspects of current measurement,
as well as the research that has resulted from data
collection and analysis. In addition, the agents of
current production have been classified under two main
headings, viz., meteorological effects and geophysical
effects. Under meteorological effects of seiche activity
and wind are considered while the effects of geological
setting, bottom topogranhy and the earth's rotation are
discussed under the heading of geonhysical influences.
(Canada Centre for Inland Waters).
Lewis, T. L. - See: R. G. Sutton, No. 373.
Lipton, S. D. - See: R. C. Bubeck, No. 4?.
255. Liu, P. C. 1970. Statistics of Great Lakes levels.
Proceedings 13th Conference Great Lakes Research.
PP. 360-368.
Spectral analysis of monthly water level data in the
frequency range of 0-6 cycles ner year reveals that
significant oeaks of annual cycles exist in all the lakes.
Spectra obtained by taking the differences between the
monthly data and long term average for the same months do
not contain any prominent peaks. Spectral analysis of
annual water level data in the frequency range between
0-1/2 cycles ner tear suggests the existence of a long
term neriodic cycle of eight years.
Loewen, P. - See: T. L. Richards, No. 316.
256. Luther, D. 0. Undated. Geologic map of the Buffalo
quadrangle. Mew York State Museum, Bulletin 99.
26 p.
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The map presented gives accurate data in regard to the
surface rocks and succession of strata at and in the
immediate melphborhood of Buffalo. The man and its
accompanying text pive a detailed guide to the rock
sections of the region and to the scattered and often
obscure outcrops of the formations.
The Buffalo quadrangle embraces geologic formations which
extend from the Upper Silurlc well into the Upper Devonic,
The rocks abound in fossils which have been cited under
their respective formation names.
257. Mack, Frederick K. and Ralph E. Digman. 1962. The
ground water resources of Ontario County, New York.
U. S. Geological Survey, Bulletin OVM8. 99 p.
Ontario County is located in the Ontario Lake Plain in
the north and the Finger Lakes region in the south. Both
the consolidated bedrock and the unconsolidated deposits
which overlie the bedrock are sources of ground water
available from any of these sources depends on the thick-
ness, lateral extent, permeability, topographic setting,
lithology and location of the aquifer.
MacKenzie, R. J. D. - See: G. C. Dohler, No. 159.
258. Martin, J. 0. 1901. The Ontario coast between Fairhaven
and Sodus Bay, New York. American Geologist. 27(6)
331-334.
In the area between Fairhaven and Sodus Bay, large bluffs
are visible from the lake. The bluffs consist of clay
and Medina Sandstone with lake beaches consisting of
gravel and boulders. Wave action apparently erodes the
bluffs from a few inches to ten feet per year. Behind
the bluffs, ponds and lagoons are formed during high
water and flow out in low lake level times. The shore-
line in the area has been eroded from 1/4 to 1/2 mile in
this area since formation of the lake as we know it
today.
Massey, D. G. - See: T. L. Richards, No. 315.
Matheson, D. H. - See: D. V. Anderson, No. 13-
259. Matheson, D. H. 1958. A consolidated report on Burlin-
ton Bay. Municipal Laboratories, Corporation City
of Hamilton, Ontario, Canada. 110 p.
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This report Includes watershed features:
1. Description.
2. Morphoinetry (water depth and area covered).
3. Ground water characteristics (chemical and physical
properties).
4. Tributaries (characteristics, size arid flow).
5. Marsh, bay and general water analysis,
6. Meteorological data (precipitation and water levels).
7. Runoff.
The general physical parameters include: temperature,
both surface and stratification and turbidity. The tur-
bidity levels indicated a serious problem with some bay
areas containing five times as much suspended matter as
the adjacent lakes areas,
260. Matheson, D. H. 1962. A pollution study of western Lake
Ontario. Great Lakes Research Division, Univ. of
Michigan, Publication 9. pp. 15-20.
Three tracers were used to study the emission and distri-
bution of polluted water from Hamilton Bay into Lake
Ontario. The pollutants studied were: ammonia, coliform
bacteria and synthetic detergent.
261. Matheson, D. H. 1963. A sanitary survey study of
western end of Lake Ontario, 1961-63- Water Works
Intakes. City of Hamilton, Ontario, Canada. 109 p.
Temperature, lake levels, sustained oscillations, currents,
winds and thermal structure were all studied by the City
of Hamilton, Ontario, during the period of 19bl-1963.
Seasonal variation was from 2^7-9 ft. in June and July
to 2*13.5 ft. In the winter months. The yearly difference
Is approximately four feet between high and low levels.
Uninodal oscillations had a period of 5.1*! hours while
that of binodal oscillations was 2.48 hours.
The currents on the surface varied with wind variation
Indicating a direct relationship between the two.
Thermal structure showed seasonal variations following
that of larger lakes.
262. Matheson, D. H. and D. V. Anderson. 1965. Circulation
and water quality of western Lake Ontario. Ontario
Department of Lands and Forests. Research Report
No. 62. pp. 1-36.
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In designing water intakes from lakes and associated
treatment plants, a knowledge of the character of the
water is useful. This is especially true where lake
waters are liable to pollution and where there are wide
daily and monthly variations in physical characteristics.
In preparation for a new intake at Hamilton, Ontario,
surveys were conducted in I960 of the waters of the lake
nearby. Measurements of circulation, temperature and of
various chemical constituents made in these surveys are
reported here,
263. McAndrews, J. H. Unpublished. Pollen analysis of the
sediments of Lake Ontario, For publication by the
2i»th International Geological Congress. Unnumbered.
Analyses were made on 91 surface sediment samples and
values were derived of both percentages and concentra-
tions (grains per gram dry sediment) of 6l taxa. Con-
centration was highest, over 80,000, in the deep-water
clays but was less than 40,000 in shallow, near-shore
silts and sands. Pollen of ragweed and tree pollen,
dominate the relatively uniform assemblage, however,
significant percentage variations reflect nearness to
upland source regions, river discharges and recycling
of sediment.
Two deep-xvater (over 180 m) cores at stations 80 km
apart penetrate 5 to 7 m of postglacial sediment and 9
to 11 m of late-glacial sediment. Eight pollen assem-
blage zones are present and correlate with radiocarbon
and varve dated pollen assemblages from sediment of
nearby small lakes. The pollen concentration of the
seven postglacial zones is 35 times greater than the
late-glacial spruce zone reflecting both greater pollen
influx and the lesser rate of matrix accumulation. The
ragweed zone begins at a depth 15 to 20 cm from the
surface and represents forest clearance around the Lake
beginning in the early 19th century. (Royal Ontario
Museum, Toronto).
26*4. McCombie, A. M. 1967. Some physical and chemical
characteristics of the Bay of Quinte. Ontario
Department of Lands and Forests, Research Branch.
Report No. 79. 56 p.
There is danger that the Bay of Quinte will become
eutrophied to the point where the fish populations are
endangered. Accordingly, the research branch of the
Ontario Department of Lands and Forests undertook to
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study certain aspects of the Phvslcs, Chemistry and
Phytoplankton of the Bay during the summers of 1963-1964,
in order to compare present Conditions with those
reported in earlier investigations, by Tucker (19^9)
and Pal (195B). Physical studies included temperature
and specific conductivities. Surface waters attain
their greatest temperature in 1 he third week cf July.
The Innermost portions of the Bay v.-ere generally warmer,
Specific conductance of the outer Bay area was generally
greater than in the inner Bay,
In conclusive, secchi disc readings were also taken.
265. McCrindle, W. E. 1961. A study of some bottom deposits
from Lake Ontario. M. S. Thesis, Department of
Geology, Univ. of Toronto. '\2 p,
Sediment samples taken from the bottom of Lake Ontario
off Scarborough Bluffs xvere subjected to mechanical and
mineralogical analyses in an attempt to shovi relation-
ships between the sediments and distance from shore,
depth of water, currents and wave action. It was con-
cluded that the sources of material deposited on the
bottom of Lake Ontario in the area studied -ire; (1)
shore erosion, (2) streams, (3) erosion on the lake
floor. Tables included show results of m.lner.-iloglcal
analysis; grain size distribution vs. distance from
shore; and heavy minerals vs. distance from shore.
(Canada Centre for Inland Waters).
Mclntyre, D. R. - See: T. L, Richards, No. 31 J.
266. McVehll, G. E., C. W. Rodgers and W. J. Eadie. 1968.
The structure and dynamics of lak* effeci-s snow-
storms. Cornell Aeronautical Laboratory, Inc.,
Buffalo, New York. Report No. VC~25t9~?-1. ^9 p.
A correlation is made between lake water parameters and
climatology to produce favorable condition;? fr*r a "Jake
effect" snowstorm. The storms generally occur or: fcne
eastern edge of a lake when a northwesterly wind Is
pushing cold arctic air over warm water of t;he lakes.
Snow characteristics are also discussed In reference to
structure and occurrence.
Megerian, E. - See: B. G. DeCooke, !Jo. 1*>1.
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267. Megerian, E. 196*4. Forecasting Great Lakes levels -
second through sixth month. Great Lakes Research
Division, Univ. of Michigan, Publication No. 11.
pp. 238-252.
A previous forecasting model presented in this series
failed to account for the adverse meteorological condi-
tions which often prevail over the lakes. The method
v.sed in this paper assumes periodic changes in conditions,
consequently the hypothetical normal values are also
changing. Hence, the most probable amount of net basin
supply can be determined on a monthly or yearly basis
utilizing trend analysis.
268. F-igerian, E. and R. L. Pentland. 1968. Simulation of
Great Lakes basin water supplies, U. S. Lake Survey,
Army Corps of Engineers, Detroit, Michigan. MP 68-2.
6 p.
'.'he basic concept utilized in the simulation study is to
evaluate statistically the recorded supplies to isolate
the two components assumed to constitute the basin water
supply: (1) That portion of the supply that is consid-
ered randon, owing to chance interaction of unpredictable
rrateorological elements, and (2) That portion of the
supply that is the result of the persistence due to
natural storage in the lakes, soil, bedrock and snow over
the drainage basin. In this study, consideration was
also given to the relationship between supplies in
neighboring basins. These factors are used to formulate
mathematical models for simulation of supplies to all of
the Great Lakes simultaneously. Extensive statistical
tests have been used to ensure that the statistical
parameters and the time series characteristics of the
simulated data resemble those of the recorded data.
269- Menon. A. S., B. J. Dutka and A. A. Jurkovec. 1970.
Preliminary studies on the effects of the Lake
Ontario thermal bar in confining bacteria to the
near-shore region. Division of Public Health
Engineering, Department of National Health and
Welfare. Manuscript Report No. KR. 70-2. 25 p.
Investigations into the thermal structure and heat budget
of Lake Ontario by G. K. Rodgers and D. V. Anderson
resulted in the discovery and identification of a
phenomenon known as a thermal bar. In May, 1970, a study
was undertaken to assess the influence of the thermal bar
in confining bacteria to the near-shore area, during the
spring period of rapid growth. The impetus for this
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bacteriological study, was the realization that the
barrier effect of the thermal bar might have serious
economic and health implications. That is, effluents
discharged into the near-shore area would not be dilutee!
as would occur under normal conditions but would be con-
tained by the barrier effect of the thermal bar.
Two preliminary studies were undertaken to investigate
the containing effect of the thermal bar. In the "time
series study," two anchor stations, one on either side
of the thermal bar, were sampled during alternate 2k
hour periods at k hour intervals for 48 hours. Para-
meters studied in this investigation were total coliforms,
fecal coliforms, 20°C MP plate count and bacterial bio-
mass .
In the second study, a tracer bacteria,
ma.Jtc.zA ccn.6 was released, 10 meters below the surface,
inshore of the thermal bar; then at varying time inter-
vals water samples were collected from mobile stations
on both sides of the thermal bar. During this study,
water samples were tested for total coliforms, 20°C MP
plate counts, S. maiceAcen* MP and S. ma/tce^cenxi
presence-absence test.
From the data collected during this preliminary study,
it could be shown that the thermal bar did have an effect
on bacterial densities in the study area. Great differ-
ences in bacterial densities and biomass were observed
between samples collected inshore and those collected
off-shore of the thermal bar. Attempts were made to
correlate diurnal changes with variations in bacterial
densities; however, during this study, fluctuations in
bacterial densities at the two ancho^ sample stations do
not appear to be linked to diurnal changes.
The feasibility of using S. marcescens to follow the
movement of bacteria in a lake was aptly demonstrated by
the recovery of the tracer organism at Station S , six
hours after being released. Recovery of S. marcescens
at the one inshore station, although suggestive, cannot
be considered supportive evidence for the suspected
barrier effect of the thermal bar. Further studies with
more intensive tracking of the tracer organism are
planned for 1971.
Prom these preliminary studies, it would appear that the
thermal bar acts as a barrier, separating the warmer more
productive Inshore waters from the mid-lake waters and
also may retard or inhibit the diffusion of bacteria from
the inshore to the offshore area.
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270. Millar, P. G. 1952. Surface temperatures on the Great
Lakes. Journal of Fisheries Research Board of
Canada. 9: 329-376.
Thermographs were installed on the intakes of several
steamships on the Great Lakes with which the HpO temp.
was recorded for 5-10 years. Averages are presented
in tables, maps and diagrams. The temperature varies
considerably over a lake surface in a manner determined
by depths and currents. Standard Deviation and serial
correlations are found for some of the data.
271. Miller, W. J. 1924. The geological history of New York
State. New York State Museum. Bulletin No. 168.
148 p.
The glacial, preglacial and post-glacial history of New
York State are discussed. The article contains data on
geology, geological formation and evolution, erosion,
glaciation and the various ice ages.
Monsinger, M. N. - See: D. C. Archibald, No. 17, 18,
19, 20, 21, 22.
Mooh, C. P. - See: E. C. Johnson, No. 226.
272. Mortimer, C. H. 1971. Large-scale oscillatory motions
and seasonal temperature changes in Lake Michigan
and Lake Ontario. Univer. of Wisconsin-Milwaukee,
Center for Great Lakes Studies, Special Report No.
12. 106 p.
Chapter 1 outlines the annual thermal cycle in Lakes
Michigan and Ontario.
The second chapter starts with a description of upwelling
in a snail lake and as modified by the Coriolis force in
Lake Ontario and Lake Michigan. Depending on wind
direction, upwelling can occur on either shore, accom-
panied by a downward tilt (downwelling) of the Isotherms
on the opposite shore. A clear correlation between
upwelling occurrences and the speed, direction and timing
of the wind stress is Illustrated for Lake Michigan. By
analogy with the generation of internal seiches by wind
in small lakes, the principal responses of Lake Ontario
and Lake Michigan to impulsive wind stresses are predic-
ted to contain large contributions from the lowest odd-
numbered, free internal (horizontal) modes, with the
proportionality of the model contributions determined by
the particular shape of the thermocline surface as
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displaced by the wind stress, and on the duration and
periodic content of the wind impulses. An increase in
Internal wave activity after storms is demonstrated.
In Chapter 3, the theory is discussed of long internal
waves in channels and basins in which rotation effects
are Important. The chapter was prepared in collaboration
with Dr. M. A. Johnson of the British National Institute
of Oceanography. Equations governing the wave motion are
given and simplifying boundary conditions and assumptions
are discussed. The solutions to the wave equation found
by Kelvin, Poincare and Sverdrup are considered. The
Sverdrup solution or wave, only satisfies the equation at
points remote from the shore. The Kelvin solution is
imposed by the presence of a boundary at x^hich the normal
fluid velocity component must be zero. Pairs of Sverdrup
waves can be combined to satisfy the boundary conditions
in a channel and two types of these are either standing
waves or progressive waves; in either case, these are
called Poincare waves. The characteristics of the various
types of wave motion are discussed in this chapter, and
their respective zones of activity are examined. In Lake
Ontario, the limitations on the present models are not
considered to be serious, but produce modifications or
damping of wave patterns as predicted by the models
discussed.
The observations in Lakes Michigan and Ontario tempera-
ture oscillations and currents are interpreted In Chapter
4, which makes up one-half of the report, and examines
the evidence of oscillatory motion in the txvo lakes.
Records of temperature at municipal water intakes on both
lakes occasionally show short bursts of oscillation, with
a period of between 14 and 17.5 hours. The slow progress-
Ion of a temperature "wave" northward past the Intakes on
the eastern shore of Lake Michigan after upwelling could
be a Kelvin wave. Near shore the currents are predomin-
antly shore-parallel and subject to rapid and frequent
reversals associated with changes in the wind. Further
offshore the rotational contributions of the Poincare
waves assume greater importance and are often dominant.
The final section demonstrates that, although a large part
of Internal wave energy in the Lakes is concentrated near
the lower frequency limit corresponding to the dominant
long wavelengths, shorter wavelengths are also conspicuous
Another concentration of wave energy occurs near a high
frequency limit, called the Brunt-Vaisala frequency,
corresponding in Lake Michigan to wave periods of a few
minutes. Possible mechanisms for the transfer of wave
energy from low to high, and high to low frequencies, are
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discussed. The most clearly established result in
Chapter 4 is the demonstration of transverse standing
wave patterns, dominated in one episode by the uninodal
and in the other by a quintinodal component. A number
of pieces of evidence combine to suggest that very long
north-south wave lengths were present.
273. Murphy, T. E. 1970. Considered Lake Erie-Lake Ontario
waterway. U. S. Army Corps of Engineers, Buffalo
District. Technical Report H-70-3. 53 p.
The Investigation reported herein was conducted to assist
the U. S. Army Engineer District, Buffalo, in determina-
tion of the economic justification of a water route
connecting Lake Erie and Lake Ontario. Specifically,
the study involved determination of the most functional
and economical location for a lock in the vicinity of
Buffalo, N. Y. and evaluation of navigation conditions
at the entrance to an overland canal Joining the American
channel of the Niagara River nortlwest of North Tonawanda,
N. Y.
An existing model of the Niagara River with a horizontal
scale of 1:360 and a verticle scale of 1:60 and a new
understarted model of the canal entrance with a 1:120
scale were used in the investigation.
Tests demonstrated the desirability of placing the new
lock in the vicinity of Buffalo as far downstream as is
feasible without rendering the existing Black Rock Lock
and Canal inoperable during the construction period.
Navigation problems at the canal entrance were not as
severe as had been contemplated and a small amount of
overexcavation resulted in satisfactory conditions.
Murthy, C. R. - See: H. S. Weiler, No. 430.
274. Murthy, C. R. 1969. Large scale diffusion studies at
Niagara River mouth, Lake Ontario. Proceedings
12th Conference Great Lakes Research, pp. 635-651.
Some results of large scale dye plume experiments con-
ducted during the summer of 1968 at the mouth of the
Niagara River are oresented. Analysis of the results
includes cross plume concentration data and certain
diffusion characteristics of the dye plume at the river
mouth. The results indicate a very rapid river mixing
fairly close to the source, followed by fairly regular
diffusion typical of a lake situation.
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275. Murthy, C. R. 1970. An experimental study in horizontal
diffusion in Lake Ontario. Proceedings 13th Confer-
ence Great Lakes Research, pp. 477-489.
During the 1969 field season, three dye patch diffusion
experiments, in early May, mid June and late August, were
conducted of the western end of Lake Ontario, as part of
a coordinated program, known as MELON (Massive effort on
Lake Ontario), to study large scale horizontal diffusion
in the Great Lakes environment. In each experiment, a
slug of water soluable rhodamine B dye in 40# acetic
acid-methanol solution was introduced into the surface
layer. The growth of the diffusing dye patch was
followed at different times for about 60 hours after dye
release using the familiar fluorometric technique. The
data covered a length scale from 100 m to 10 km.,and the
corresponding eddy diffusivities varied from 10 to 105
cm /sec. a diffusion characteristic prepared from the
data suggests that the horizontal eddy diffusity grows
as the 4/3 power of the length scale in accordance with
the results of the similarity theory of turbulence.
276. Murthy, C. R. and G. T. Csandy. 1971. Outfall simula-
tion experiment in Lake Ontario. Abstract of paper
presented at the l4th Conference Great Lakes
Research, Toronto, Ontario, April 19-21, 1971.
p. lol.
In order to obtain some experimental evidence on diffu-
sion, rhodamine dye (B) was released in Lake Ontario,
near Oshawa, in water 20 m deep, 3 meters from the
bottom, from 10 m long diffusion pipe arranged horizon-
tally. The intention was to carry out surveys of the
resulting plume for prolonged periods (10 days).
Vertical sections across the dye plume were regular.
Horizontal distributions in contrast were many peaked,
mostly very much wider than comparable dye plumes near
the surface, and in some places consisted of only dis-
crete patches of dye, hundreds of meters distant. These
features of diffusion may be attributed to wave-like
character of flow at low residual velocity.
277. Newberry, J. S. 1870. On the surface geology of the
basin of the Great Lakes and the valley of the
Mississippi. Annals Lyceum of Natural History.
9: 213-234.
Topographic and geologic data for the Great Lakes -
Mississippi Valley areas are presented, including pro-
perties and structures, location, occurrence, formation,
evolution and local characteristics.
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278. Newberry, J. S. 1882. On the origin and drainage of the
basins of the Great Lakes. Proceedings American
Philosophical Society, Philadelphia, pp. 91-101.
A general discussion by the author of the origin and
drainage of the basins of the Great Lakes is accompanied
by an objective discussion of the glacial theories of
erosion by Mr. Leslie. The topography, geology, drainage,
age, evolution and characteristics of the basin are all
discussed.
279. Newland, D. H. 1933- The Paleozoic stratigraphy of New
York. International Geological Congress, l6th
Session. Guidebook 4, Excursion A-1*, Washington,
D. C. 136 p.
A paper written for an excursion throughout New York
State. Various distinct areas of geologic formations
are separated and analyzed for geology, climatology,
topography and stratigraphy.
280. New York State Atomic and Space Development Authority.
Undated. A thermal Drofile of the waters of New
York State. Albany, New York. 27 P-
The technique of infrared aerial scanning is utilized to
ascertain surface water temperatures of Lake Ontario and
many of the major waterways of New York State. The
currents, winds and waves have various mixing and dis-
persion characteristics which can be followed easily by
high altitude infrared scanning.
281. New York State Department of Health. 1957. Lake Ontario
drainage basin series, Eighteen Mile drainage basin.
NYS Department of Health, Albany, Report No. 3.
71 p.
A comprehensive biological, physical and chemical study
of the Eighteenmlle Creek Drainage Basin and other tribu-
taries entering Lake Ontario between the NiagaraRiver and
Eighteenmile Creek. The physical parameters from this
NYS Health Department report include: temperature, pre-
cipitation, topographic maps, stream locations and flow
direction, volume, variation and levels, water sources,
industrial and domestic uses, classification of shoreline
areas, water color, odor, turbidity and suspended matter,
geological land formations, stream and lake sampling
stations.
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282. New York State Department of Health. 1958. Lake Ontario
Drainage Basin Survey Series, Lake Ontario surface
waters, including specified tributaries. NYS Depart-
ment of Health, Albany, N. Y. , Report No. 4. W p.
A comprehensive biological, physical and chemical study
of Lake Ontario and its tributaries. The physical para-
meters include: temperature, precipitation, topographic
maps, stream locations and flow, water sources, Industrial
and domestic uses, flow direction, volume, variation and
water levels, classification of shoreline areas, water
color, odor turbidity, suspended matter, geological land
formations, stream and lake sampling stations.
283. New York State Department of Health. 1961. Lake Ontario
Drainage Basin Series, Upper Genesee River drainage
basin. NYS Department of Health, Albany, N. Y.,
Report No. 2. 219 p.
A comprehensive biological, physical and chemical study
of the Upper Genesee River Drainage Basin, The physical
parameters from this NYS Department of Health report
Include: temperature, precipitation, topographic maps,
stream locations and flow direction, volume, variation
and levels, water sources, industrial and domestic uses,
classification of shoreline areas, water color, odor,
turbidity and suspended matter, geological land formations,
stream and land sampling stations.
Nunez, M. - See: J. A. Davies, No. 1^5.
284. O'Connor, D. J. 1959. Statistical analysis of drought
flows of rivers of New York State. New York State
Water Pollution Control Board Research, Albany,
N. Y., Report No. 1. 6l p.
On many rivers in the state, flow gauging stations are
maintained by the U. S. Geological Survey. These
stations and the published records of stream flow gently
assist in the conductance of the water pollution surveys
and classifications. Statistical analysis of the low
flows may be made, from which a drought of any severity
may be estimated. This report proposes to:
1. present the cumulative frequency distributions of
drought flov/s so that a low flow of any desired
frequency may be determined directly.
2. determine which of the three commonly employed dis-
tributions is most appropriate for such analysis in
order to establish a basis for future work.
3. generalize the major drainage basins or geophysical
areas in the state.
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Of field, T. W. -- See: D. W. Fisher, No. 1?2.
285. Oliver, W. A., Jr. 195^. Stratigraphy of the Onondage
limestone (Devonian) in Central New York. Bulletin
Geological Society of America. 65: 621-652.
Detailed studies of the distribution of fossils in the
Onondaga limestone (Devonian) in central New York permit
division of the formation into four members each of which
is subdivided into two or more zones and several lateral
fades. The Edgecliff (lowest) member is a coral blo-
strome over much of the State but locally passes into a
bloherm facies. A basal zone of reworked sand (Spring-
vale of various authors) is included in the Edgecliff
whereever present. The Nedrow member is a shaly limestone
characterized by a variety of platyceratid gastropods.
The upper part of the member is a more massive limestone
with a sparse fauna. The Nedrow passes westward into
cherty limestone with few fossils and wastward into coarse
limestone. The Moorehouse member is a massive, fine-
grained limestone characterized by abundant brachipods
and certain large colled cephalpods. This member passes
west and east to coarser limestones with brachipod-coral
founas. The base of the Seneca (upper) member is defined
as the "Tioga bentonite," a prominent marker bed and an
Important paleontologlc break. The Seneca is character-
ized by an abundance of CA.one^te-6 £x'.nea-tu4 and a few other
forms. The Seneca member passes to the east into the
Union Springs black shale of the overlying Marcellus
formation. This relationship is indicated by the east-
ward thinning of the limestone and thickening of the
black shale unit, and by the eastward disappearance from
the top down of the Seneca zones which are recognized in
the type area.
286. Ontario Water Resources Commission. 1962. Report on
a lakefront survey of water quality, waste outfalls,
and drainage inlets of Lake Ontario within the area
town of Burlington to Scarborough township, inclu-
sive. Ontario Water Resources Commission., Toronto.
142 p.
Tabulated data are presented for Canada on tne surface
water of Lake Ontario along the shoreline from Burling-
ton to Scarborough on: water temperature, suspended
solids and turbidity. Descriptive statements are made
for each sampling location. These statements include
date and location of sampling and weather conditions.
(Canada Centre for Inland Waters).
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287. Ostry, R. C. 1971. Hydrology of the Forty Mile Creek
drainage basin on the south shore of Lake Ontario.
Abstract of paper presented at l^th Conference
Great Lakes Research, Toronto, Ontario, April 19-21,
1971. pp. 170-171.
The forty mile creek drainage basin is considered to be
typical of the ground water regime developed in the
Niagara Peninsula area and has been studied as a part of
the International Field Year on the Great Lakes program
to assess the ground water contribution to Lake Ontario.
The results of this hydrogeologic study are as follows:
1. The ground water divide to a depth of approximately
150 feet below the ground surface appears to be the
same as the surface divide.
2. Two ground water flow systems were deliniated and
have been designated as local and regional.
3. Ground water discharge from the regional system is
influenced by the topographic relief associated
with the Niagara escarpment.
4. Apparent velocities of ground water movement are
3000 feet per year in Silurian bedrock and approxi-
mately 100 feet per year in the underlying formations
5. Water quality deteriorates rapidly across the basin
from the divide to the stream channel and also with
increasing depth.
6. Direct ground water discharge in the area per mile
length of Lake Ontario is In the order of 6000 Igpd.
288. Owen, E. B. 1969. Stratigraphy and engineering des-
cription of the soils exposed on a section of the
Welland Canal by-pass project (contract 7^3).
Ontario, Canada Department of Energy, Mines and
Resources. Geological Survey of Canada. Paper
69-31. 22 p.
The methods and procedures used to forcase excavation
requirements in the Welland Canal by-pass project are
outlined. Comparison is made between geological condi-
tions inferred before excavation and the conditions
actually encountered by the contractor.
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289. Pach, A. B. 1963. The heavy snows at Watertown, N. Y.
Weatherwise. 16(2): 66-67, 78.
The winter of 1962-1963 had an abnormally heavy snowfall,
snow cover, and persistently cold temperatures (January
average was below 3°F - February average below 8°P) near
Watertown, New York. The snow caused economic problems
and the weight of the snow mass collapsed several roofs.
The article includes a general accumulation discussion,
but no explanation.
Fade, B. - See: G. T. Csandy, No. 142, 143.
Paine, D. A. - See: J. E. Jiusto, Mo. 225.
290. Palmer. M. D. 1968. Currents in Frenchman Bay area of
Lake Ontario. Ontario Water Resources Commission,
Toronto, Ontario. Unnumbered.
Two recording current meters were operated from June to
August, 1968 in 12.7 m (42 feet) of water at distances
of 2.42 m (8 feet) and 4.6 m (15 feet) from the bottom
approximately 1.6 km (1 mile) offshore in the Frenchman
Bay area of Lake Ontario. A time series analysis was
carried out on the resulting data for the various months.
A maximum current of 21 cm/sec. (0.69 fps) observed was
significantly lower than results obtained by similar
current meter studies in adjacent areas and farther off-
shore. This appears to be a result of the shore geometry
which reduced the currents in the area. Both the direc-
tions and persistence factors agree with results of other
studies. Wind does not appear to be directly responsible
for currents in the area which are produced as a result
of diurnal, inertial and Lake Ontario free oscillation
effects. The thermal regimes were a direct consequence
of inertial effects. (Canada Centre for Inland Waters).
291. Palmer, M. D. 1969. Simulated thermal effluent into
Lake Ontario. Proceedings 12th Conference Great
Lakes Research, pp. 674-485.
The dispersion pattern of Duffin Creek water into Lake
Ontario was determined under two different wind condi-
tions in the spring time when the flow was used to trace
the plume by continuous dye injection. The flow was 180
cfs and the water was 5°F warmer than the lake water.
Based upon experimental results, a model was developed
which predicts maximum concentrations within 25% for
distance up to 4000 feet from source. Maximum dye
concentrations varied as the (distance) -0.8. The
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model applied to an existing thermal generating station
at Lakeview was capable of predicting maximum tempera-
tures within 25% of measured values.
292. Palmer, M. D. 1971. Estimate of the physical extent of
thermal plumes at Lakeview, 1971. Ontario Water
Resources Commission, Toronto. 31 p.
The cooling plumes from an operation thermal electric
generation plant station at Lakeview, west of Toronto,
on Lake Ontario, were defined by water temperature
measurements. The generating station discharged between
1400 to 2500 cfs of cooling water at 15°P. above intake
water temperatures. The temperature measurements were
made throughout the year at various depths in proximity
of the discharge to define the physical cooling water
plume in the lake. Equations were developed which defined
plume area as a function of distance from the discharge,
temperature as a function of plume area and plume centre-
line as a function of wind. Different relationships were
developed for summer and winter conditions based upon the
ambient lake temperature. The most significant cooling
resulted from mixing with lake water. (Canada Centre
for Inland Waters).
293. Palmer, M. D. and J. B. Izatt. 1970. Lakeshore two
dimensional dispersion. Proceedings 13th Conference
Great Lakes Research, pp. ^95-507.
Hourly two dimensional dispersion characteristics are
determined from recording current meter histories for the
nearshore areas of Lakes Erie and Ontario. The current
histories were obtained in areas within 4 km of shore and
at water depths of 10-lU m during May to December, 1968.
A markov chain process was applied to hourly current
readings. Three different formulations of the stochastic
process were tested prior to the selection of the most
reliable one. The results obtained in applying the
developed technique were compared favorably with the
results obtained form conventional dye injection and
dropue studies.
294. Paskausky, D. P. 1971. Winter circulation in Lake
Ontario. Abstract of paper presented at 14th
Conference, Great Lakes Research, Toronto, April
19-21, 1971. pp. 21-22.
In winter, Lake Ontario is in a barotropic or homogeneous
fluid circulation mode. A barotropic, prognostic, numeri-
cal circulation model, which Includes topographic,
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Inertial, lateral and bottom friction and wind stress
terms, is applied to Lake Ontario. The circulation
pattern is determined for tvro cases; first, the river
inflow and outflow only and second with both river flow
and wind field that could be produced by a meteorological
high pressure area to the southeast of the Lake.
Pentland, R. L. - See: E. Magorian, No. 268.
295. Pentland, R. L. 1968. Hydrologic statistics and lake
level regulation. Abstract of paper presented llth
Conference Great Lakes Research, Univ. of Wisconsin,
Milwaukee, Wisconsin, p. 36.
Maps showing the distribution of runoff are presented
for the entire Great Lakes Basin on a monthly and annual
basis. Computerized methods have made possible the
utilization of more than 250 hydrometric stations within
and surrounding the basin for each of the thirteen runoff
maps. A geographical representation of the area-runoff
distribution for the subbasin is also presented. The
paper includes a general discussion of the effects of
climatological and physical features in relation to the
runoff characteristics.
296". Pentland, R. L. and N. E. Eryuzlu. 1969. A dynamic pro-
gramming algorithm for the operation of the Great
Lakes. Department of Energy, Mines and Resources,
Inland Waters Branch. Reprint Series No. 53- 24 p.
In Great Lakes regulation studies currently being conduc-
ted by the International Joint Commission, the economic
consequences of many regulation plans are being evaluated
by various agencies who have a direct interest in the
outcome of the studies. A wealth of economic data has
been gathered which enables the determination of benefits
or detriments of any given plan of regulation in each
particular interest for each lake and for each country
(Canada and the United States). A dynamic programming
algorithm is used to facilitate the development of
operating policies. A number of short cuts and approxi-
mations are required due to the magnitude of the
investigation. The scope of the problem is discussed
along with some of the methods used to reduce computing
costs to reasonable proportions.
Peterson, C. P. - See: R. L. Drake. No. 162.
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297. Phillips, D. W. 1971. The modification of surface air
over Lake Ontario in water. Abstract of paper
presented at 14th Conference Great Lakes Research,
Toronto, Ontario, April 19-21, 1971. p. 60.
Climatological and. synoptic studies of the Great Lakes
and their basins have always suffered from a scarcity of
data over the lakes. This is especially true of the
winter months from December to April when a few ships
move out of port. This study provides a method of
estimating the extent to which surface temperatures and
humidities are modified in passing over Lake Ontario
during the cold months. Temperatures, cloud height and
amount, wind direction and speed, and air pressure were
measured. The difference between the air teaperature
on land and water temperature of the sample site at the
ship was used as an index of stability and the over
water fetch was measured. An index of "time over water"
t;as computed by combining the fetch distance and wind
speed.
298. Pincus, J. H, 1959- Great Lakes basin. American
Association Advancement of Science, Washington,
D. C. Publication No. 71. 308 p.
An extensive book produced by the combination of many
articles by different authors pertaining to the various
aspects of the Great Lakes Basin. The following articles
pertaining to physical characteristics are presented.
Geologic Framework - J. L. Hough
Drainage and Climate - W. E. Powers
Water Balance of the Great Lakes System -
J. P. Bruce
Great Lakes Waters, Their Circulation and
Physical and Chemical Characteristics -
J. C. Ayers
Regimen of the Great Lakes and Fluctuations
of Lake Levels - W. T. Laidly
Recession of Great Lakes Shorelines - H. J. Pincus
Surface and Groundwater Supplies in Ontario -
A. K. Watt
Water Pollution in the Great Lakes - A. H. Dahl
Great Lakes Water Supply - The Years Ahead -
H. W. Posten
(Canada Centre for Inland Waters).
299. Pohlman, J. 1884. The life history of the Niagara
River. Proceedings American Association Advance-
ment of Science, 32d Meeting, p. 203.
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Lakes Erie and Ontario once stood at the same height at
one tine (that of Lewiston Heights). As Lake Ontario
drained, the channel from the whirlpool to Lewiston was
easily eroded. The channel of the river above the whirl-
pool was part of the old river flowing between the two
lakes but was bottled up by the last glacier. Therefore,
the age determinations of the glacial retreat versus
erosion time are always too great because the erosion
distance was not from Lewiston to the present site of
the falls at Niagara.
300. Pohlman, J, 1887. The Niagara Gorge. Abstract of paper
presented in the Proceedings American Association
Advancement of Science, 35th Meeting, pp. 221-222.
The Niagara Groge was cut originally by three separate
falls. The lower (downstream) two having softer sand-
stones to erode, receeded at a much faster rate
eventually catching the upper falls which was eroding
harder limestone and receedlng slower. The St. David
Gorge was bottled up by the last ice retreat forcing
the river to flow down a channel previously flowing
into the river at the present whirlpool site.
301. Pound, A. 19^5. The American Great Lakes series - Lake
Ontario. Bobbs-Merrill Co. Publishers, Indianapolis,
Indiana, p. 235-345.
A historical survey of the Lake written in lay terms
including Indian history and wars.
Part 3 contains data on counties, cities and industries
along the lake shore. It also includes some data of
history of Niagara Palls and prominent landmarks.
302. Powers, C. and A. Robertson. 1966. The aging Great
Lakes. Scientific American. 215(5): 3-10.
Aging process increases are discussed in relationship
to eutrophication and siltation. Lake Ontario has
increased in dissolved solids in the last 50 years
approximately 50 ppm.
303. Prichard-Carpenter. Undated. Drift and dispersion
characteristics of Lake Ontario nearshore waters,
Rochester, New York to Sodus Bay, New York.
Rochester Gas and Electric Corporation, Rochester,
N. Y. 23 p.
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Drift and dispersion studies were conducted in Lake
Ontario during April-May, July and October, 1965. The
study area was along the south shore of the lake between
Rochester and Sodus Point. The drift was found to be
primarily wind induced, with speeds and direction. A
steady drift to the east of 0.05 knots was present during
calm periods.
Tracer material was released continuously at the Brookwood
site during the study periods. The observed distributions
of released material were fitted to theoretical equations.
The probable distributions of heat and material released
with the condenser cooling water flow under different dis-
charge structure designs were computed from the observed
diffusion data. These computations show that the use of
a horizontal Jet minimized the thermal effect and produced
the most rapid dilution of constituents, so that a Jet
(approximately 2 ft/sec) discharge should be considered
as optimum. With horizontal discharge, significant heat-
ing would not be present along the lake shore beyond the
site boundary and the area with temperatures elevated
by 5 degrees would extend out into the lake approximately
3000 feet and have an average width of 200 feet.
The study showed that a twenty-fold or greater dilution
would occur before the discharge reaches the area of the
nearest public water intake (town of Ontario). This
intake is located on the bottom at a depth of 11 feet.
Thirty-fold dilution would be expected before the dis-
charge could be drawn into the plant intake located on
the bottom at a depth of 28 feet. (Canada Centre for
Inland Waters).
Putnam, D. F. - See: L. J. Chapman, No. 96, 97, 98, 99.
304. Radforth, I. 19^1. Some considerations on the distri-
bution of fishes in Ontario. M. A. Thesis, Depart-
ment of Zoology, Univ. of Toronto. 119 p.
Included is a section on the geologic history of the
principal drainage systems of Ontario. Glacial retreats
and the formation of the Great Lakes are both discussed.
(Univ. of Toronto, Zoology Library).
305. Rafter, G. W. 1905- Hydrology of the State of New York.
New York State Museum Bulletin 85. 902 p.
Data are given for all major lakes and river systems in
New York State. Meteorological data are given on a
yearly basis and include: temperature, pressure,
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humidity, precipitation and wind velocity. Mean air
temperature and precipitation are discussed on a monthly
basis also. Each water system is Isolated and analyzed
for topography, geology, volume flow, flow characteristics
and drainage area.
306. Rainey, R. H. 1967. Natural displacement of pollution
from the Great Lakes. Science. 155(376?): 1242-
1243.
A simplified mathematical model of a lake system indicates
that, if the pollution of the Great Lakes were discontin-
ued, the natural flow through the lower Great Lakes would
be sufficient to remove about 90 percent of the waste in
about 20 years. On the other hand, hundreds of years
vrould be required to displace the pollution from Lake
Michigan and Lake Superior.
307. Rao, G. V. 1971. A numerical analysis of a potential
snow squall situation over Lake Ontario with a
primitive equation model. Abstract of paper pre-
sented at the 14th Conference Great Lakes Research,
Toronto, Ontario, April 19-21, 1971. p. 63-64.
The purpose of this diagnostic study is to provide on a
preliminary basis the three-dimensional structure of a
potential snow squall saturation x^ith the aid of a con-
sistent system of dynamical equations and approximations.
Wind and geopotential heights were plotted on a large
area base map covering most of North America. Geopoten-
tial, isotach and streamline analyses were subjectively
performed. The analyses over Lake Ontario then were
transferred to a local area base map. The Initial fields
of motion and temperature over the local area were cal-
culated following the procedures sketched by earlier
investigators.
308. Repp, R. D. 1970. Ailing Niagara Palls. Water Spectrum.
1(2): 32-38.
Discussion of the study conducted by the Army Corps of
Engineers of the American section of Niagara Palls. A
cofferdam was constructed at the southern end of Goat
Island blocking the American Channel. The Corps was
then able to undertake a geological investigation of
Palls materials and erosion. Faulting and stresses were
measured by borings and electronic sensing equipment.
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309. Richards, T. L. 1963a. The meteorological factors
affecting Great Lakes water levels. Canadian Depart-
ment of Transport, Meteorological Branch. Circular
4182, Tec. 553, Toronto. 22 p.
The Great Lakes are subject to large and varied fluctua-
tions in water levels. Most of these are due to
meteorological factors; - wind and pressure are respon-
sible for short-term variations, precipitation and
evaporation for annual and longer-term changes.
Man-made alterations, such as diversions and channel
deepenings, have resulted in lake level changes that are
small compared to those caused by meteorological factors
except in Lake Huron/Michigan where a significant down-
ward crend since i860 is apparent. (Univ. of Toronto,
Great Lakes Institute.
310. Richards, T. L. 1963b. Meteorological factors affecting
ice cover on the Great Lakes. Great Lakes Research
Division, Univ. of Michigan. Publication 10: 204-
215.
Freezing and thawing degree day data from a 14 year
record were used to calculate average and extreme ice
conditions that may be expected from the lake. The depth
of the lake has a direct effect on the formation, reten-
tion and dissipation of ice cover and in the case of a
deeper lake (such as Lake Ontario), will actually reduce
ice cover. Reduction of ice cover is a much more rapid
process than the formation of ice and requires a much
smaller change in temperature.
311. Richards, T. L. 1964. Recent developments in the field
of Great Lakes evaporation. Verh. Internat. Verein.
Limnol. 15: 247-256.
The research program of the Great Lakes Institute's
research ship is described including, the limnological
and meteorological parameters measured and the processing
of data. Evaporation over the Great Lakes was studied.
Micro-profiles of data obtained by the ship's meteorolo-
gical boom are being assessed although this method of
obtaining data has limitations. Data were also collected
to establish lake-land ratios for Humidity Ratio H and
Wind Ratio R. These ratios permit climatologlcal data
from shore stations to be adjusted to make monthly lake
evaporation estimates using the Mass Transfer Method.
Evaporation figures for Lake Ontario were calculated this
itfay and comparisons are made with other methods. Sugges-
tions for refining the ratios are made.
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312. Richards, T. L. 1969. The Great Lakes and the weather.
Great Lakes Institute, Univ. of Toronto. PR-39.
p. 10.
The subject of the Great Lakes and the weather is a very
broad one and indeed includes much more than might be
apparent at first glance. That the almost 100,000 square
miles of water surface making up the system has a power-
ful influence on the weather may be confirmed by any one
of the 50 million inhabitants living in the region. How-
ever, at least as important is the fact that individual
weather elements also have a tremendous influence on the
Lakes themselves, i.e. winds cause waves and shore damage,
currents affect the distribution and dispersal of pollu-
tants, freezing temperatures bring ice and an end to
navigation and precipitation and evaporation combine to
cause very large and economically important variations In
water levels. As a result, this review will consider
both aspects of the Interaction between the Great Lakes
and the weather. (Canada Centre for Inland Waters).
313. Richards, T. L. , H. Dragert and D. R. Mclntyre. 1966.
Influence of atmospheric stability and over-water
fetch on winds over the lower Great Lakes. Monthly
Weather Rev. 9^(7):
Five years of wind observations taken by the research
vessel C.C.G.S. Porte Dauphlne on Lake Erie and Lake
Ontario have been compared to simultaneous observations
taken at land stations upwind of the ship. The resultant
ratios of over-lake winds/over-land winds have been sorted
by speed classes, conditions of atmospheric stability and
the length of the over-water fetch to assess the relative
influence on each factor on the over-lake wind.
The effect of changes in atmospheric stability as created
by air-water temperature differences is shown quantita-
tively with results confirming that wind speeds increase
over water during unstable conditions and decrease during
stable conditions. It is also shown that these changes
are greatest in low winds and least in high winds.
An increase in the length of the over-water fetch up to
about 25 mi. contributes to an increase in wind speeds
during unstable conditions. Under very stable conditions
the lake winds become lighter with longer fetches but
the changes are highly erratic. This is likely due to
Intermittent breakdowns of the shallow atmospheric
inversion layer associated with the stable conditions.
An increase in fetch beyond 25 mi. does not appear to
contribute to any further change in speeds.
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314. Richards, T. L. and J. P. Fortin. 1962. An evaluation
of the lake-land vapor pressure relationship for
the Great Lakes. Great Lakes Research Division,
Univ. of Michigan. Publication 9, pp. 103-110.
Several methods have been used in recent years for the
quantitative determination of evaporation from a large
body of water. One classic approach is the Mass Transfer
Method involving a water vapor flow formula. 705 synop-
tic hour observations were used from Lakes Ontario, Erie,
Superior and Huron to help redevelop the equation and
modify it to fit the size of the Great Lakes basin.
315. Richards, T. L., J. G. Irbe and D. G. Massey. 1969-
Aerial surveys of Great Lakes water temperature,
April 1966-March 1968. Canada Department of Trans-
port, Meteorological Branch, Cllmatological Studies.
Mo. 14. 55 P.
Extensive aerial survey data are presented on all the
Great Lakes from a series of 82 ART surveys. Depth,
temperature gradients, surface temperatures, mixing and
diffusion studies are discussed and shown in maps of the
Great Lakes.
316. Richards, T. L. and P. Loewen. 1955. A preliminary
investigation of solar radiation over the Great
Lakes as compared to adjacent land areas. Great
Lakes Research Division, Univ. of Michigan.
Publication 15, pp. 278-281.
This preliminary Investigation includes observations
from sectors of Lakes Ontario, Erie, Huron, and Superior
within 100 miles of Sault Ste. Marie, Cleveland and
Toronto during the months of April to December inclusive
and presents the comparisons as monthly ratios of total
radiation over water to total radiation over land.
Results based on data collected since I960 confirm the
physical concept of substantially greater incoming solar
radiation over the lakes during the summer (due to less
cloud cover over the water areas) with the opposite
effect particularly evident in the early spring and late
fall.
317. Richards, T. L. and G. K. Rodgers. 1964. An investiga-
tion of the extremes of annual and monthly evapora-
tion from Lake Ontario. Great Lakes Research
Division, Univ. of Michigan. Publication 11, pp.
283-293.
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The modified mass transfer method, provides a useful
technique for examining evaporation from a large lake.
In this particular study a number of contributions have
been made towards a better understanding of the evapora-
tion process as It concerns Lake Ontairo:
(a) A method has been developed to translate daily
intake temperatures into realistic mean monthly surface
water temperatures.
(b) Average evaporation estimates for Lake Ontario have
been calculated for the 14-year period 1950-1963, con-
firming previously reported characteristics of the annual
evaporation cycle.
(c) Evaporation estimates have been calculated on a month
to month basis over a 14-year period. The maximum,
minimum and standard deviations of these estimates produce
an indication of the variability of evaporation from Lake
Ontario not previously available.
(d) A direct comparison of month to month averages of
wind speed, vapour pressure and surface water tempera-
tures with evaporation estimates for the same months
points up the relative importance of these meteorological
parameters in the evaporative process. As noted earlier,
better evaporation estimates will come from a better
understanding of the lake and the atmosphere above it,
assisted by the continued acquisition of data - be It by
research vessels, lake towers, networks of buoys or air-
craft observations.
Rickard, Lawrence V. - See: J. G. Brought on, No. 39.
Rlckard, L. V. - See: D. W. Fisher, No. 172.
318. Rickard, L. V. 1964. Correlation of the devonian rocks
in New York State. NYS Museum and Science Service
Geological Survey. Map and Chart Series No. 4.
1 sheet.
Contains a large map and accompanying tables of the
devonian rocks in New York State. The various geological
eras are discussed along with geology, stratigraphy,
evolution, erosion and topography.
Robertson, A. - See: C. Powers, No. 302.
Robinson, P. J. - See: J. A. Da vies , No. 145.
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Robison, F. L. - See: P. E. Greeson, No. 192.
319- Robison, F. L. 1969a. Floods in New York-196?. U. S.
Geological Survey Report Of Investigations RI-3,
Albany, New York. 32 p.
This report presents information on floods reported in
NYS during the calender year of 196?. Special emphasis
is placed on cause, date, location, volume discharge
accidents and damage caused by flooding.
320. Robison, F. L. 1969b. Floods in New York-1968. U. S.
Geological Survey Report of Investigation RI-9,
Albany, New York. 30 p.
This report presents information on floods reported in
NYS dueing the calendar year of 1968. Special emphasis
is placed on cause, date, location,volume discharge,
accidents and damage caused by flooding.
321. Rockwell, D. C. 1966. Theoretical free oscillations of
the Great Lakes. Great Lakes Research Division,
Univ. of Michigan. Publication 15, pp. 352-369.
The lowest five modes of longitudnal free oscillation of
each of the Great Lakes are investigated by numerical
intergration of the hydrodynamical channel equations.
The corresponding periods, surface profiles and volume
transports are presented and discussed. The fundamental
periods are: Lake Superior-?.2 hrs; Lakes Michigan/
Huron-47.8 hrs; Lake Michigan-8.8 hrs; Lake Huron-6.5
hrs; Lake Erie-l4.1 hrs; and Lake Ontario 4.9 hrs.
Special consideration is given to Lakes Michigan and
Huron in connecting these lakes through the Straits of
Mackinac.
Rodgers, C. W. - See
Rodgers, G. K. - See
Rodgers, G. K. - See
Rodgers, G. K. - See
Rodgers, G. K. - See
Dodgers, G. K. - See
G. E. McVehil, No. 266.
D. V. Anderson, No. 11, 14.
J. P. Bruce, No. 43, 44.
P. F. Hamblin, No. 200.
T. L. Rickards, No. 317.
W. G. Simpson, No. 351.
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322. Rocgers , G, K. 1959. Temperatures and currents near
jhore in the Longbuneh-Port Credit area. Ontario
Dept. of Lands and Forests, Physics Research Note
No. 7: 3. 4 figures.
This article covers the following topics:
(a) Surface temperature - surface temperatures measured
in 1958 on the long branch shoreline never exceeded 70°F.
To aUow approximate extrapolation to toner seasons the
tempera v.ire of water coming in the Slow Sand Intake of
t^f: Toronto Island, Toronto Water Works plant is plotted
in Figure 4. This intake is at a depth of about 40 feet.
Of special note is the frequent intrusion of cold water
during the summer months.
<',t<) Temperature structure - water along this shoreline is
stratified in the summer. There was always a nearly homo-
geneous upper layer (homogenous in temperature) of at
least 20 feet in deoth during July and August. This
homogenous layer (epillimnlon) is shallower than most of
the open lake. Below this layer, in the thermocline,
tr.fi temperature decreased with gradients ranging from
t*Mo to 10 P degrees in about 10 feet. Thus, during July
and M'p-nst the water at 40 feet was five to ten degrees
cr-iiiej' than surface water.
In the fall, stratification was much less marked and the
water ir-ore nearly homogeneous in tempearture. Thus,
while surface temperatures were relatively well maintained
at a surp.nier level, temperatures at 40 feet were more near-
ly equal to surface temperatures and hence temperatures
at [iC fee; -I v/ere often higher in September than during
July
a;ni August .
(c) Surface currents - currents measured in the surface on
27 November were in the same direction as the wind, and
the exception is that surface currents are determined by
•che wind In this area. The surface currents in lakes are
Principally w'r,d controlled is a fact confirmed by many
oDaervers (Rut chins on, 1957).
The Climatologlcal Atlas of Canada Indicates that prin-
cipal wind directions in winter at Toronto are W, SW, NW
and K. In summer, winds are evenly distributed around
the compass with the exception of a lower frequency of
winds from the SE. Thus, average surface littoral cur-
rencs throughout the year should, in this area, tend to
flow easterly, although the evidence is by no means
conclusive, (Univ. of Toronto, Zoology Library).
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323. Rodgers, G. K. 1962. Lake Ontario data report. Great
Lakes Institute, Univ. of Toronto. PR-7. 102 p.
This publication contains limnological and meterological
data collected annually by the Great Lakes Institute.
Information contained in the report Includes the follow-
ing parameters in the following categories.
1. Meteorology - wind velocity and direction, tempera-
ture, humidity, clouds, waves.
2. Radiation data.
3. Limnology data - surface temperature, waves,
turbidity, gradients, conductivity.
4. Bathythermography traces.
32*!. Rodgers, G. K. 1963. Lake Ontario data report. Great
Lakes Institute, Univ. of Toronto. PR-10. 192 p.
This publication contains limnological and meterological
data collected annually by the Great Lakes Institute.
Information contained in the report Includes the follow-
ing parameters In the following categories.
1. Meteorology ~ wind velocity and direction, tempera-
ture, humidity, clouds, waves.
2. Radiation data
3. Limnological Data - surface temperature, waves,
turbidity, color, temperature gradients.
4. Bathythermograph traces.
325. Rodgers, G. K. 1966a. A note of the thermocline
development and the thermal bar in Lake Ontario.
Symposium of Garda, International Association
Scientific Hydrology. 1(70): 401-405 .
Lakewide temperature observations in Lake Ontario have
been made during the spring when the thermocline is
forming and the thermal bar is present in the lake.
Examination of heat content changes in the central,
deepest parts of the lake reveals that advection of
warm surface water from areas nearer shore plays a
significant role in the development of the major thermal
stratification in these deeper areas once the thermal bar
has paased. Waters formed in the thermal bar become
summer hypolimnlon.
3?6. Rodgers, G. K. 1966b. The thermal bar in Lake Ontario,
spring 1965 and winter 1965-66. Great Lakes
Research Division, Univ. of Michigan. Publication
15, pp. 369-374.
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The temperature and water masses of Lake Ontario were
studied during the spring and winter periods when waters
are present at temperatures both above and below the
temperature of maximum density. The zone where the
surface v;as Just at the temperature of maximum density
(the thermal bar) separating these waters demonstrated
marked horizontal gradients in temperature, turbidity
and color. The movement of the thermal bar is documented
for the tiering condition and current measurements taken
in the bar are shewn.
Jvodgers, G. K. 1968. Heat advection within Lake Ontario
In spring and surface water transparency associated
with the thermal bar. Proceedings llth Conference
Great Lakes Research, pp. 481-^86.
The pattern of heat content changes throughout Lake
Ontario during the period in which stratification
developed (April through June) in the spring of 1965
suggests that advection of warm water from shore areas is
an important factor in the formation of the thermocllne
on the shore r.ide of the thermocllne.
Previous papers on the thermal bar have described the
high correlation of turbidity with temperature at the
lake surface in the region of the 4° isotherm, based on
visual reports. Records of crossing this Isotherm in
1967 with a towed transmissometer thermometer confirm
the correlation quantitatively and also reveal in detail
the associated variety of horizontal temperature gradients.
328, RodgerSj G. K. and D. V. Anderson. 1961. A preliminary
study of the energy budget of Lake Ontario. Journal
of Fisheries Research Board of Canada. 18(^1) : 617-
636.
Recent bathythermographic surveys carried out on the
research vessle Porte Dauphine have provided estimates
of heat content for Lake Ontario and permitted a pre-
liminary study of its energy budget. The imbalance
between the absorbed short wavelength sun and sky radia-
tion, and the loses due to evaporation, sensible heat
conduction and net long wave length back radiation result
in heating of lake water from March to August and cooling
from September or October to February. The peak heat
content lags the peak surface temperature by about one
month. The amount of energy advected into the lake is
relatively small compared with other terms In the evergy
budget. Thus, energy budget calculations do not depend
upon the accuracy with which the water budget is known.
-------
The principal difficulty in applying present techniques
for determination of an energy budget is lack of meteoro-
logical data over the lake surface.
32?. Rodgers, G. K. and D. V. Anderson. 1963. The thermal
structure of Lake Ontario. Great Lakes Research
Division, Univ. of Michigan, Publication 10. pp.
59-70.
A lakewide survey of Lake Ontario is discussed indicating
seasonal changes in layering and all over energy dynamics.
The total energy of the lake follows a lag pattern behind
the temperature changes over the various seasons.
330. Rodgers, G. K. and A. H. Lee. 1971. Temperature
inversions in Lake Ontario. Abstract of paper pre-
sented at 14th Conference Great Lakes Research,
Toronto. April 19-21. pp. 212-214.
For a temperate dimlctlc lake such as Lake Ontario, a
temperature inversion refers to either an increase or
decrease of water temperature with depth for waters near
4°C, such that in the absence of pressure effects, the
temperature variation with depth would result in a state
of static instability.
Parameters discussed are: frequency of occurrance,
magnitude of the Inversion, thickness of the inversion
layer, depth of the temperature maximum or minimum,
regional distribution, seasonal distribution and verticle
and horizontal stabilities.
331. Rodgers, G. K. and G. K. Sato. 1970. Factors effecting
the progress of the thermal bar of spring in Lake
Ontario. Proceedings 13th Conference Great Laices
Research, pp. 9^3-950.
Evidence is presented supporting the contention that the
primary control of thermal bar movement lies with surface
heating and the initial heat content of the "cold" section
of the lake into which the thermal bar moves.
In a discussion of what constitutes the beginning of the
thermal bar, two regimes are identified. The first is
the progress in the development of the thermocline in
the whole lake, and is controlled primarily by surface
heating and initial lake temperatures in the deep part
of the lake. The second type of thermal bar arises due
to flow of waters greater than 'I°C into the lake at
temperatures less than 4°C.
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332. Rodgers, H. D. 1835. On the falls of Niagara and some
authors opinions respecting them. American Journal
of Science and Arts, 27: 326-333.
A basic discussion of the falls at Niagara is presented
involving location, dimensions, viewpoints, general
river characteristics, basic geology, evolution and age.
Rondy, D. R, - See: R. Wilshaw, No. 435-
333. Rondy, D. R. 1966. Great Lakes ice cover - winter 1965-
66. U. S. Lake Survey, Army Corps of Engineers,
Detroit, Michigan. Report 5-2, M p.
This report represents the 22 ice charts obtained by the
U. S. Lake Survey observers on 12 ice reconnaissance
flights. Made during the 1965-66 ice season. These
flights covered a distance of about 9,775 statute miles
and all ice-covered areas of the Great Lakes xirere
observed. Maximum ice cover for each of the lakes
occurred during the last two weeks in February. Esti-
mates were: Lake Superior - 605?, Lake Michigan - 15$,
Lake Huron - 2Q%, Lake Erie - 855? and Lake Ontario - 105?.
During most of the winter 1965-66 a general northwestward
shift of the storm tracks and blocking conditions created
by pressure systems to the north contained the southern
movement of the artic air mass. These blocking condi-
tions caused air temperatures to be above normal in the
Great Lakes area and contributed to a shorter than
expected period of ice cover. (Canada Centre for Inland
Waters.)
35''. Rondy, D. R. 1967. Great Lakes ice cover - winter 1966-
67. U. S. Lake Survey, Army Corps of Engineers,
Detroit, Michigan. Report 5-3, 54 p.
Eighteen flights were made over areas of the Great Lakes
to record ice conditions during the 1966-67 winter.
Data collected on these flights are presented on forty
ice charts.
Weather conditions over the Great Lakes in general during
the winter of 1966-67 were characterized by frequent
fluctuations of temperatures that averaged near normal.
Ice was first reported forming on Lake Superior during
the last week of November and on Lake Erie during the
last week of December. The maximum ice cover was
during the first week in March on Lake Erie and
-1U6-
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the third week of March on Lake Superior. During the
period of maximum ice cover Lake Superior was estimated
to be 88 percent covered with the ice varying from heavy
winter ice in the Duluth, Port Arthur and Whiteflsh Bay
areas to 9/10 concentration of brash and floes in mid-
lake; Lake Michigan, 46 percent covered with heavy
winter ice in Green Bay and that area to the north and
east of Beaver Island and various concentrations of
brash and cake along the southern perimeter; Lake Huron
80 percent covered with heavy winter ice in the North
Channel, Straits of Mackinac and Saginaw Bay; while the
central basin was almost ice free all season; Lake Erie
85 percent covered with heavy winter ice in the form of
consolidated brash and cake in the eastern and western
basin; and Lake Ontario 12 percent; here the ice cover
was confined to the eastern end and approaches to the
St. Lawrence River. Ice was reported on Lake Superior
as late as 16 April while on the same date the other lakes
were comparatively ice free (Canada Centre for Inland
Waters).
335. Rondy, D. R. 1968. Great Lakes ice cover - winter 1967-
68. U. S. Lake Survey, Army Corps of Engineers,
Detroit, Michigan. Report 5-4, 10 p.
Thirty-eight ice charts were produced from data collected
on 14 reconnaissance flights made during the 1967-68
winter season.
Ice was reported forming in the Duluth, Minnesota area of
Lake Superior as early as 12 November and on Lake Erie
along the western shore as early as 16 November. During
the period of maximum ice cover Lake Superior was esti-
mated to be 90JJ ice covered with approximately equal
areas of winter and young ice; Lake Michigan 30 percent
ice covered with most of the ice concentrated in Green
Bay and the island area in the north end of the lake;
Lake Huron 50 percent covered with winter ice In the
North Channel, Georgian and Saginaw Bay areas; Lake Erie
98 percent covered with young and winter ice. The
eastern basin and the approaches to Buffalo Harbor con-
tained large Jammed areas with many windraws. Lake
Ontario 10 percent, with the ice confined in general to
the various channels to the northeast. In May ice was
still being reported in the Black Bay area along the
north shore of Lake Superior and on the Buffalo area of
Lake Erie as late as 3 May.
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336. Rondy, D. R. 1969a. Great Lakes Ice atlas. Great Lakes
Research Center, Army Corps of Engineers, Detroit,
Michigan. 6 p. + 35 charts and tables.
A short article with extensive mapping on the accumulation,
composition, properties of and dissipation of ice on the
Great Lakes. The great depth and small surface area of
Lake Ontario produce conditions unfavorable for ice for-
mation because the central deep water mass resists extreme
thermal changes and usually does not reach the freezing
point. If ice does appear, it is quickly dissipated by
winds. The ice cover extent is; 8% mild winter, 15% in a
normal winter, and 25% on a severe winter. (Canada Centre
for Inland Waters).
337- Rondy, D. R. 1969b. Great Lakes ice cover - winter 1962-
63. U. S. Lake Survey, Army Corps of Engineers,
Detroit, Michigan. Report 5-5, 33 p.
Eleven flights were made over areas on the Great Lakes
during the winter 1962-63 resulting in the publication
of fourteen ice charts. During the winter 1963-64,
seventeen ice charts were produced from ten flights,
The U. S. Weather Bureau rated the winter of 1962-63 as
one of the most severe in 100 years with temperatures
across the Great Lakes region as much as 8°P below normal.
By comparison, the winter of 1963-64 was warmer with tem-
peratures averaging 2°P below normal in the south and 3°F
above normal in the north. The temperature deviations
from the normal for the winters of 1962-63 and 1963-64
are indicated by graphs of .2 freezing degrees-days for
each of the lakes.
The ice cover on the lakes varied considerably during
these two winters. Lake Superior had the greatest var-
iation in ice cover with a difference of 64 percent in
aerial extent between the winters of 1962-63 and 1963-64.
Maximum ice cover.
Rukavlna, N. A. - See: R. G. Sutton, No. 374, 375.
Rukavina, N. A. - See: D. L. Woodrow, No. 436.
338. Rukavina, N. A. 1967- Rapid inspection of soft sediment
cored by x-radlography. Proceedings 10th Conference
Great Lakes Research, pp. 143-148.
X-radlography provides a fast and non-destructive method
for the preliminary inspection of unconsolidated sediment
cores. Test radiographs of several cores from Lake
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Ontario Indicate that adequate definition of sedimentary
structure is obtained when cores are radiographed in
their plastic liners. This approach permits soft sediment
structure to be recorded before it is distorted or des-
troyed by extrusion, and eliminates the conventional
sample preparation for radiography. Preliminary results
of a comparison of radiography density with sediment
parameters Indicate that density is a function of water
content (porosity), which is in turn related to particle
size „ organic content and consistency.
339. Rukavlna, N. A. 1969* Nearshore sediment survey of
western Lake Ontario, methods and preliminary
results. Proceedings 12th Conference Great Lakes-
Research, pp. 317-32^.
Surface sediment samples, echo sounder profiles, and.
bottom observations by divers and with underwater
television are being used to map the sediments and bottom
morphology of nearshore Lake Ontario (depth 0-20 m). In
1968 mapping was completed in the western end of the Lake
from Niagara, on the south shore to Whitby on the north
shore.
Six bottom types have been recognized arid deliniated:
1) bedrock-23^, 2} glacial drift-39/? and the recent
sediments, 3) gravel and pebbly sand-9$, *0 sand-12%,
5) sllt-sand-10*, 6) sllt-clay-7*.
Recent sediments occur: 1) on the south shore from
Niagara to Jordan, 2) on the west shore opposite the
Burlington Bar, 3) on the south shore opposite metro-
politan Toronto. The deposits at Toronto and Niagara
result from local erosion shore bluffs; westward moving
longshore currents supply the sediment accumulating off-
shore from the Burlington Bar.
Rukavina, N. A. 1970. Lake Ontario nearshore sediments
Whitby to Wellington, Ontario. Proceedings 13th
Conference Great Lakes Research, pp. 266-273.
Mapping was based upon bottom samples, echo sounder
records and underwater television observations.
Three bottom types were identified and deliniated:
1) glacial sediment and lag deposit 55%, 2) sand 25%,
3) bedrock 20%. Glacial material occupies the major
portion of the zone x^est of Colborne. Bedrock is exposed
east of Colborne. The major sand deposit occurs in the
area surrounding the Presquile Peninsula. Elsewhere the
sand is restricted to the vicinity of creek mouths or
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entrances. Sand Is contributed to the zone by stream
discharge, bluff erosion and submarine erosion. Met
transport Is in an eastward direction and accumulation
occurs in the vicinity of Presquile.
341. Sanderson, M. 1971. Variability of annual runoff in the
Lake Ontario basin. Abstract of paper presented
14th Conference Great Lakes Research, Toronto.
April 19-21, pp. 95-96.
The present study of variability of runoff in the Lake
Ontario basin provides background information for the
International Field Year on the Great Lakes In 1972,
since it is realized that a period of 1 year is a small
sample In the life history of a lake basin and there are
large annual fluctuations In the variables In the water
balance. In their study of the hydrology of Lake Ontario,
Morton and Rosenberg concluded that most of the annual
variation in water level Is caused by variation in the
net basin supply. The largest variable Increasing the
basin supply Is the runoff averaging 46 to 56 inches com-
pared to evaporation of 24 to 36 Inches, and precipitation
of 28 to 32 Inches.
Sato, G. K. - See: G. K. Rodgers, No. 331.
3^2. Schutze, L. T. 1966. Determination of flow over Niagara
Palls. U. S. Lake Survey, Army Corps of Engineers.
Bulletin B66-1, pp. 1-9.
By a treaty signed in 1950 the flow of water over Niagara
Falls cannot be reduced beyond certain values by the
Niagara Palls Power plants. The variations in flow
caused by the power Intakes have a significant effect on
currents, water depth and velocity flow of water in the
lower Niagara River. Mathematical Models and formulas
are used In flow and diversion variation analysis.
(Canada Centre for Inland Waters).
Scott, J. T. - See: U. H. Czapskl, No. 144.
Scott, J. T. - See: D. R. Landsberg, No. 243.
343. Scott, J. T., P. Jekel and M. Fenlon. 1971. Transport
in the coastal current near the south shore of Lake
Ontario In early summer. Abstract of paper presen-
ted at 14th Conference Great Lakes Research,
Toronto, 19-21 April, p 45.
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In early summer, the currents along the south shore of
Lake Ontario, are primarily barocllnlo and concentrate
in a fairly narrow band or "coastal jet," These boundrj/
modified coastal currents are generally set up by the
relatively strong winds following the passage of summer
cyclones and cold fronts. The paper describes a study
of the transport and pattern of a coastal current which
resulted from a typical summer storm on July, 1970.
Current velocity and temperatures were measured to *JQ m
depth. Dynamic height patterns, cross sections of tem-
perature and computed baroclinic gees trophic velocity all
showed spacial and temporal consistency for the six day
period.
The coastal current was the major consistent feature of
the circulation pattern. The six day means of the
measured and computed transport were nepriy the same
indicating that the steady coastal current in ,,,ake
Ontario is primarily baroclinic in early summer.
Scott, J. T. and D. R. Landsberp. 1969, July currents
near the south shore of Lake Ontario. Proceedings
12th Conference Great Lakes Research, ~-^ , f05~?22.
Drogue Measurements of current direction and speed at
five anchored buoys near the south shore of Lake Ontario
from 11-20 July 1968 near Fairhaven, M. Y. , showed that
total transport in the 35 m layer was north-eastward
along the shore. However, at stations 1 anc? : km from
the shore there v;as a southwestward flowing ''c
current." The maximum northeastward coastal .j
normally located from 6-10 km from shore
geostrophic transport was computed from dall
was
llnle
ir,pera-
ture soundings at 10 stations. Internal wjivea and wind
fluctuations did not mask the baroclinic Keosi-ropMc
flow for this near shore case. Baroclinic gee 5 trophic
flow and total transport were to the northeast lr, the
surface layers, but the analysis indicated thr" there vws
a slow return flow opposed to these.
Transport in deep water was, therefore, southv.ost.i. ar-d.
The baroclinic geostrophic computation was c. i^ccl ,.ro -
dictor of surface currents in summer when the- la tier arc
much larger than the steady return barotrophrlc. flow.
345. Scott, J. T. and L. Lansing. 196?, Gradient, on relation
in eastern Lake Ontario. Proceed:! ngs 10th Confer-
ence Great Lakes Research, pp. 322-336.
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Thermal patterns in eastern Lake Ontario are examined
to determine themagnitude and cause of baroclinicity
which produces gradient (nearly geostropic) currents.
A strong gradient current flows eastward along the
south shore and northward along the east shore In early
summer. This current is probably caused by a combina-
tion of local heating due to differences in lake depth
and coastward advection of warm surface water by Eckman
transport. Evidence of persistent baroclinicity in late
summer was not found but may have been masked by verticle
displacement of the strong thermocline.
346. Scovell, J. T. 1890. An old channel of the Niagara
River. American Association Advancement of Science.
39th Meeting, pp. 245-246.
It is believed that the waters of Lake Erie formally
flowed into Lake Ontario by a channel some miles west of
their present course, and that the retreating glacier
so obstructed this old channel that the waters were
compelled to take a new course forming the Niagara River.
Geologists believe the time between the present and the
glacial retreat is approximately 10,000 years.
347. Simons, T. J. 1971. Development of numerical models of
Lake Ontario. Unpublished paper presented at 14th
Conference Great Lakes Research, Toronto, April 19-
21, 1971. p.6-7.
At the Canada Centre for Inland Waters, a program has
been initiated to simulate the ivater motion in Lake
Ontario by numerical models. The program consist of
evaluating existing numerical techniques, developing an
hierarchy of models describing the circulation of the
lake under various conditions and an extensive verifica-
tion program for the purpose of evaluating the degree of
accuracy of the various models by comparison with the
abundance of observational data to become available during
the year 1972.
Simpson, R. B. - See: D. V. Anderson, No. 15-
348. Simpson, R. B. and D. V. Anderson. 1964. The periods
of the longitudnal surface seiche of Lake Ontario. Great
Lakes Research Division, Univ. of Michigan, Ann
Arbor. Publication 11, pp. 369-381.
Proudman's method allows calculation of the period of a
seiche from the actual configuration of a lakes basin.
This method has been adapted to automatic computation
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and used to determine the uninodal and binodal periods
of the longitudnal surface seiche of Lake Ontario.
These are 5.4l and 2.48 hours, respectively.
3^9. Simpson, R. B. and D. V. Anderson. 196?. The surface
tides of Lake Ontario. Ontario Department of Lands
and Forests. Research Report No. 76. 42 p.
This report describes work started by Dr. Anderson when
he was with the Department of Lands and Forests.
Monthly averages of surface levels, at successive hours,
reveal the lunar and solar tides of Lake Ontario. The
relative amplitudes and phases in the eastern, central
and western basins are in accord with theory. It is
suggested that intensive tidal studies will help unravel
puzzles in circulation and that they may be useful in
constructing correlations with seasonal meteorological
changes.
350. Simpson, W. G. and G. K. Kamltakahara. 1971. Opinions
on recreation and pollution in Lake Ontario. Univ.
of Toronto, Great Lakes Institute. 10 p.
Data collection techniques are used to ascertain pollu-
tion levels in various parts of the lake.
351 Simpson, W. G. and G. K. Rodgers. 1970. Currents in
Lake Ontario near Toronto. Proceedings 13th Con-
ference Great Lakes Research, pp. 528-539.
Current measurements have been made for 4 years at one
location in 10 m of water near Toronto. A summary of
these data, in time series and frequency distributions,
end a relacJon between current and wind, found by an
e.aphencal analysis are given. 'This relation permits
prediction of currents at this location.
352. Sissons, J. B. 1966. Subglacial, marginal and other
glacial drainage in the Syracuse-Onelda area, New
York. Bulletin of the Geological Society of
America. 71: 1575-1588.
In his numerous papers on central New York, H. L. Falr~
child interpreted almost all the glacial-drainage
features as of marginal origin. In the Syracuse-Oneida
areaa however, there is morphological evidence of sub-
glacial stream erosion by both local and Great Lakes
•vaters, of subglacial deposition by local waters, and of
onglacial flow in places. Evidence also indicates that
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the Great Lakes waters In some places flowed in channels
walled by ice. Only limited evidence of ice-dammed lakes
exists in the Syracuse-Onelda area itself, except at the
lowest altitudes, where numerous small shore features
indicate a former local lake above the highest Iroquois
shore line. There is evidence of two periods of Great
Lakes drainage across the hillslopes of the Syracuse-
Oneida area during the oscillatory retreat from the
Wisconsin maximum. The writer suggests, however, that
these two periods of Great Lakes drainage alone are
insufficient to account for the vast, complex channel
system.
353. Slater, G. 1969. The structure of the drumlins exposed
on the south shore of Lake Ontario. NYS Museum
Belletin No. 281. 16 p.
The drumlins on and adjacent to the southern shore of
Lake Ontario are unusual size and development.
The sections are usually transverse and lie across the
exposed or "leeward" ends of the drumlins.
Two phases of structure are shown, marked by a gradual
change in the lithology. A lower "core" of stiff boulder
clay passes gradually into bedded material above, con-
sisting of stoneless clays, loams and boulder clay,
associated in some cases with "wisps" and lenticles or
streaky sand.
The "core" has acted as an obstruction to the passage
of later material, resulting in the accretion of new
material, which has moved along "glide" or thrust planes,
thus producing suitable gradients. Pressure has occurred
both longitudinally and laterally, the former being
predonlmant.
35;J. Sly, P. G. 1969. Sedimentological studies in the
Niagara frea of Lake Ontario and in the area
immediately north of the Bruce Peninsula and
Georgian Bay. Proceedings 12th Conference Great
Lakes Research, pp. 341-3^6.
A study of the bottom sample variance in different
environments in the Great Lakes was begun in 196?. By
the end of 1969, two areas will have been completely
surveyed; one around the Niagara River Mouth on Lake
Ontario, and the other around Georgian Bay, near the
tip of the Bruce Peninsula. A preliminary study of
the third area in Lake Ontario near Kingston, is to
-------
begin in 1969. A special sampling grid, covering an
area of about 150 km has been devised for use in all
the study areas and sampling has been designated to yield
material for sedlmentological studies, geochemical and
biological studies. Underwater photography has been used
to provide visual records of the lake bottom. Echo
sounding, side scan sonar, and continuous seismic pro-
filing has b-en used to obtain sub-bottom penetration
and complete physiographic coverage.
355. Smith, H. M. 1892. Report of an investigation of the
fisheries of Lake Ontario. Bulletin U. S. Fisheries
Commission. 10: article 6. pp. 177-215.
A section included in this article covers such physical
characteristics of Lake Ontario as: temperature, depth,
sediment, currents and winds. They are discussed as to
their relationship with the fish in the area.
356. Spencer, J. W. l882a. A short study of the features of
the region of the lower Great Lakes during the great
river age: or notes on the origin of the Great
Lakes of North America. Proceedings American Asso-
ciation Advancement of Science, 30th Meeting, pp.
131-1^6,
The author follows the origin of several great rivers and
their altering patterns before, during and after the
glacial ages. The Great Lakes xvere formed by a complex
system of evolution involving river and glacial processes.
357. Spencer, J. W. l882b. Terrances and beaches about Lake
Ontario. American Journal of Science. 24 (3d Ser-
ies): 409-416.
The author concentrates on the Western end of Lake
Ontario to analyze the location, characteristics, prop-
erties and structures and occurrences of lake beaches
above the present water level of Lake Ontario. The
author recommends an extensive analysis to determine
ancient lake level variation and possible centlmental
movements along with the accompanying geological evolu-
tion of the region.
358. Spencer, J. W. l889a. The Iroquois Beach. A chapter
in the geological history of Lake Ontario. Trans-
actions Royal Society of Canada, Section 1C. pp.
121-134.
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Variation in beach height indicates great warping of the
earths crust in recent times. Charts of location and
elevation variation are presented. The geological history
of beach formations and the accompanying lake levels
reveals much of the glacial and past glacial history of
Lake Ontario. Much of the beach material are products of
erosion. The estimated age of the beach is 14,000 to
15,000 years.
359. Spencer, J. W. l889b. Notes on the origin and history
of the Great Lakes of North America. Proceedings
American Association Advancement of Science, 37th
Meeting, pp. 197-199.
The discussion of the evolution of the Great Lakes basin
includes: discovery of the ancient course of the St.
Lawrence River, Origin of the Great Lakes basins, estab-
lishment and dismemberment of Lake Warren, discovery of
the outlet of Huron-Michigan-Superior Lake into Lake
Ontario, by the Trent Valley and Erie, the youngest of
all the Great Lakes.
360. Spencer, J. W. 1890. Ancient shores, boulder pavements
and highlevel gravel deposits in the region of the
Great Lakes. Bulletin of the Geological Society of
America. 1: 71-86.
The discussion in this article includes: ancient Great
Lakes shoreline characteristics, comparison of ancient
and and modern shoreline characteristics, boulder pave-
ments and ancient beaches, accumulation of ancient
boulders, distribution of surface boulders,, high level
gravel deposits in the Great Lakes region, drift buried
gravel deposits and surface gravels and sands.
36l. Spencer, J. W. 1891. High level shores in the region
of the Great Lakes and their deformations. The
American Journal of Science. 3d Series. 41: 201-
211.
An investigation of high beaches, fossils, sediments and
topography has led the author to believe the levels of
the Great Lakes were once much higher than the present
lakes are. The author lists the various lakes, the high
beaches and evidence and then estimates the highest
levels attained by these lakes.
362. Spencer, J. W. 1894. Deformation of the Lundy Beach
and Birth of Lake Erie. American Journal of
Science. 3d Series. M?(270): 207-212.
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Article on the formation of Lake Erie followed chronolo-
gically through various geologic ages. Secondary infor-
mation is presented on some aspects of Lake Ontario
formation and geology.
j63. Spencer, J. W. 1895 a. The duration of Niagara Palls
and the history of the Great Lakes. Humboldt
Publishing Company, Hew York. 126 p.
The geology (preglacial, glacial and post glacial aspects)
of the Great Lakes basin region with emphasis on proper-
ties and structures, formation, age and erosion. (Royal
Ontario Museum).
364. Spencer, J. W. l895b. The geological survey of the
Great Lakes. Proceedings American Association
Advancement of Science, 43rd Meeting, pp. 237-248.
Discussion of the Great Lakes basin includes: problems
and progress, former high continental elevation, lake
basin characteristics, glaciation, the buried Lawrentian
Valley, buried tributaries, reversal of the ancient
drainage of the Ohio and other rivers, closing of the
valleys into the lake basin, deserted beaches in the lake
region and their deformation, Warren water and the birth
of the lakes, Algonquin and Fundy waters, Iroquois water-
birth of the modern lakes, drainage of the Great Lakes
into the Mississippi by way of Chicago and the history
of the Niagara River and changes of the outlets of the
lakes.
365. Spencer, J. W. l898a. Another episode in the history of
Niagara Palls. American Journal of Science, 4th
Series. 6: 439-450.
Discussion in this article includes: the changing
physics of the river, a revision of the episodes of
Niagara River, the newly discovered episode, the Niagara
Strand, the modern episode, the rise of the Ontario
waters, and explanation of the narrows of the gorge at
the Whirlpool Rapids.
366. Spencer, J. W. l898b. Another episode in the history of
the Niagara River. Abstract of paper presented at
American Association Advancement of Science, 4yth
Meeting, p. 299.
This paper is a sequel to the one read before the
American Association four years ago on the duration of
Niagara Falls. It announces the discovery that while
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the falls were receding from Foster's flats to the locality
of the railway bridges, the fall of the river reached its
maximum amount of 420 feet by the retreat of the Ontario
waters toward the north; and that, during the later part
of this recession of the falls, past the Whirlpool rapids,
the return to the present amount of 326 feet descent was
interrupted by the rising of the level of the lake In the
gorge to a height of 75 feet above its present level, thus
reducing the actual fall of the river to 250 feet. The
evidence of this is preserved In the remains of a terrace
deposit opposite the foot of Foster's flats and a corres-
ponding terrace Just outside the mouth of the gorge; and
these terraces, with other parts of the shore line in the
Ontario basin which marks the rise of the waters so as to
flood the Niagara Gorge, are here named the Niagara strand.
The rising of the waters was occasioned by the lifting of
the barrier at the outlet of Lake Ontario to an elevation
100 feet higher than now. By the subsequent erosion of
this barrier, which was partly composed of drift, the
actual fall of the Niagara waters has been Increased to
its present figure.
The reduction in the descent of the river Is found to be
sufficient to account for the shallowness of the channel
at the Whirlpool rapids. The narrowness of this section
is explained by the fact that the youghful Niagara took
possession of a small preglacial valley there, giving
greater depth to the river. It is further probable that
the volume of the river was less at that time, since it
is supposed that a portion of the outflow of the Great
Lakes passed to the Mississippi.
3^7. Spencer, J. W. 1907. The falls of Niagara. Canadian
Department of Mines, Geological Survey Branch,
Ottawa. 490 p.
A discussion of the evolution or formation of the falls
and the varying relationship to the Great Lakes. Also
Included is a discussion of power uses and diversions
•,;ith the accompanying effect on the flow volume and
asthetic value of the falls. (Schoellkopf Museum,
Niagara Falls, New York).
368. Spencer, J. W. 1917. Origin and age of the Ontario
shoreline. American Journal of Science. Series 4.
43: 359.
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The modern beach of Lake Ontario is the last of the shore
lines about the lake basin to be studied with sufficient
precision for writing its history. Much attention has
been given to the higher water D.lanes, especially to the
Iroquo:? s beach, not only shifting the lake at a high level
but tilted by subsequent earth movements, so that .is now
rises 540 ft. between the h = af of the lake and the Galops
Rapids of the St. Lawrence River (66 miles below the lake
outlet), which form the first rocky barrier to the lake
basin. In sinking from the higher beach, the waters
fell to more than 200 ft. below the present level (at
Niagara River), before the warping of the earth's crust
raised the barrier to the lake basin, so the waters rose
to a few feet above the present Ontario shoreline, from
which they have since been lowered, owing to the scour of
the St. Laxvrence River after the river sunk within its
channel.
The age of the Ontario Beach is about 2,000 years, while
the age of the lake itself and the St. Lawrence River is
3,500 years, or perhaps slightly less.
Sporns, U. - See: D. V. Anderson, No. 11.
Stewart, R. - See: U. H. Czapski, No. 144.
369. Stewart, R. 1969. Thermal discharge from nuclear plants
and related weather modification. Proceedings 12th
Conference Great Lakes Research, pp. 488-491.
The volume of thermal discharge from power plants is
increasing at a rate which suggests that the discharge
will cause inadvertent weather modification. A 10-5 M.W.
nuclear nower plant uses approximately 10 gal/min. of
which 10 gal/min. evaporates. This is sufficient to
reduce visibility and incraase fogging in the area of
discharge. Beneficial uses of thermal discharge are
suggested and calculations are presented to Indicate
that waste heat released by a dry closed-circuit-cooling
system is sufficient to dissipate fog and Increase visi-
bility. An example is used in the Lake Ontario shoreline
near Rochester.
370. Storr, J. P. 1963- Surface currents on Lake Ontario
between Oswego and the eastern end of the lake for
period of June, July and August 1963. Great Lakes
Research Division, Univ. of Michigan. Publication
11. p. 390.
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The effluent of Oswego River was used to trace the curren
(chloride analysis - 100-200 times that of lake water).
The continuity of this data, as well as the availability
of a continuous record of wind direction and force makes
it possible to trace each change in the current pattern
and to relate these changes directly to wind direction and
to relate these changes directly to wind direction and
velocity. A chronological account of the current pattern
is presented with emphasis in the 3 basic patterns of the
current complex and various phenomena that were encountered,
371. Straw. A. 1968. Late pleistocene galcial erosion along
the Niagara escarpment of southern Ontario. Bulletin
of Geological Society of America. 79: 889-910.
A large number of re-entrants in the Niagara Escarpment,
severly indenting the outcrop of the Lockport-Amabel
dolomite, are defined and their morphologic characteris-
tics are believed to have been induced largely by glacial
agencies, and various ice movements over the Niagara scarp
during the Wisconsin Glaciation are determined from a con-
sideration or moraine and drumlin trends and meltwater
drainage lines. Three maln;phases of ice advance and
recession within the Late Wisconsin and a general advance
within the Early Wisconsin are envisaged, during which ice
repeatedly flowed along and probably greatly enlarged many
of the re-entrant valleys.
Large-scale glacial erosion is demonstrated along the
Niagara scarp where it fronts onto Georgian Bay, and com-
parison is made between this area and the Finger Lakes
region in New York state. Less intense erosion is con-
sidered to have affected the remainder of the scarp,
though the Dundas valley is also regarded as a major
glacial trough. These conclusions weigh heavily against
contentions that recognizable "preglacial" features per-
sist along or in front of the Niagara Escarpment, and a
brief re-evaluation of previously postulated "preglacial"
drainage system Is made.
372. Stupart, R. F. 1913- IV. The climate of Toronto. In:
Faull, J. H. (ed.). The Natural History of the
Toronto region. Canadian Institute, Toronto, p.
82-90.
Toronto's climate is affected by Lake Ontario due to its
position on the shore of the lake. Meterological elements
discussed are temperature, precipitation, winds and baro-
metric pressure. (Royal Ontario Museum, Toronto).
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Sutton, R. G. - See: D. L. Woodrow, No. 436.
373. Sutton, R. G., T. L. Lewis and D. L. Woodrow. 1970.
Near shore sediments in southern Lake Ontario, their
dispersal patterns and economic potential. Proceed-
ings 13th Conference Great Lakes Research, pp. 309-
318.
The southern Lake Ontario near-shore consists of boulders
and till (75%), and bedrock (10/S), and sand and gravels
(15%). Potential economic sand deposits in excess of
100 million cubic yards occur at Niagara, Rochester and
along the eastern shore. Smaller deposits occur at Hamlln
Beach and Mexico Bay. Elsewhere, the sand forms small
isolated patches.
The beach sands are generally restricted to areas adjacent
to stream mouths or spits and bars extending across the
fronts of bays and ponds where effects of the prevailing
easterly currents are locally reduced. The sand fine lake-
ward and are displaced by muds in depths of over 50 ft.
15 m) and at offshore distances greater than two miles
(3.2 km). The sands generally fine from west to east.
The average sand is composed of quartz, feldspar, rock
fragments and heavy minerals (7%). Most of the sand
originated from erosion of submerged tills, till cliffs
and streams.
374. Sutton, R. G. and N. A. Rukavina. 1965. Changes in the
level of Lake Ontario as inferred from offshore
sediments at Broddock Heights, New York. Proceedings
of Rochester Academy of Science. 11(2): 72-82.
The Department of Geology at the University of Rochester
undertook an exploratory survey of the Lake Ontario near-
shore bottom near Braddock Heights, New York. The lake
currents in the area were generally moving west to east
with a decrease in strength corresponding with greater
depth. Particle size in the lake sediments should
decrease as depth increased. If the lake rises, finer
material will settle over coarser material. The survey
discovered an area approximately twenty-five feet deep
where a higher percentage of course material was discov-
ered leading to the conclusion that the lake has risen
24-30 feet from the initial beach area.
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375. Sutton, R. G., N. A. Rukavina and E. L. Towle. 1965.
Lake Ontario shoreline processes and evolution att
Braddock Heights, New York. Report of progress.
Great Lakes Research Division, Univ. of Michigan,
Publication 13, PP. 240-2H7.
Two types of sand can be identified in the offshore of
Lake Ontario near Braddock Heights, New York. One occurs
in deeper waters and is rather poorly sorted, coarser
grained and contains a high percentage of fines. The
second type is well sorted, finer grained and occurs in
shallow water. The first type is deposited in deep water
at times of storm activity; the second is a product of
wave action and longshore currents from the northwest.
Cores reveal an organic rich layer that represents older
bay deposits when the lake level rose. Drumlins that
flanked the older bay were eroded away and their sites
are marked by boulders.
The planned construction of an artificial shoal in the
study area will afford a unique opportunity to study the
changes in sediment distribution resulting from the
modified current and wave patterns.
376. Sweers, H. E. 1968. Structure of the thermocline during
the summer in Lake Ontario, llth Conference Great
Lakes Research, Milwaukee, Wisconsin, p. 45.
The Great Lakes Division, Department of Energy, Mines
and Resources, collected, among other data, a large
number of temperature observations on Lake Ontario
during the 1966-67 field seasons. These data have been
analysed with special attention to the horizontal dis-
tribution of the depth of the thermocline and the
verticle temperature structure. Persistent and transient
patterns in the lakewide distribution of the depth of the
thermocline are pointed out and an effort has been made
to interpret changes in this pattern in terms of trans-
port phenomena and to relate them to the windfleld. The
intensity of the maximum verticle temperature gradient is
discussed and related to wind strength, depth of the
thermocline and depth of the lake at the sampling station.
377. Sweers, H. E. 1969. Structure dynamics and chemistry of
Lake Ontario. Department of Energy, Mines and
Resources, Ottawa. Manuscript Report Series No. 10.
227 p.
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Data obtained from a series of monitor cruises on Lake
Ontario during the 1966-6? field seasons are analyzed.
A study of the thermal regime is analyzed utilizing the
rare natural versus random variability analysis of the
data. Thermal stratification development, characteris-
tics and dissipation are discussed with special reference
to upwelllngs, regional temperature anomalies in relation
to wind and river flows, mixing and any deviations from
the normal.
A flushing model is perfected along with the development
of an equation to calculate eddy diffusivity. Seasonal
heat content changes are calculated. The lake during the
summer months is concluded to be well mixed horizontally.
378. Sykes, R. B. 1964. Lake weather phenomena (LWP) Oswego,
N. Y. Area Progress Report. Great Lakes Research
Division, Univ. of Michigan. Publication 11, p.
321.
Progress report summarizes the Oswego area approach to
study of the snow features of the Lake Weather phenomena.
1963-64 observations from the southeast side of Lake
Ontario revealed some interesting examples of widespread
convection over the lake accompanied by some curious
mammatiform clouds at low levels. Checks with people
living near the lake for several years suggest some
uncommon aspects about certain forms and distributions
of clouds this season.
379. Taylor, B. 1895. Niagara and the Great Lakes. The
American Journal of Science. 49(Series 3): 249-270.
A lengthy discussion of the formation of the Great Lakes
basins and their respective evolution. The existence of
preglacial rivers is thought to be the factor resulting
in the original basin formation. Alterations due to
glacial advances retreats and deposits established and
altered the entire flow system until the general topo-
graphy of modern times was established. Much information
is presented on the origin, evolution and effect on Great
Lakes levels, of the development and changes in the
Niagara River.
Taylor, P. B. - See: P. Leverett, No. 249.
Taylor, P. B. - See: E. M. Kindle, No. 237.
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380. Taylor, P. B. 1898. Origin of the gorge of the whirl-
pool rapids at Niagara. Bulletin of the Geological
Society of America. 9: 59-84.
For as much of the Niagara gorge as is brought under
discussion in this paper, the correlations between the
gorge and the lakes seem clear and complete, point for
point and episode for episode. They may be summarized
briefly as follows:
1. The episode of the Middle Great gorge, extending
from Wintergreen fait up to the upper side of the Eddy
basin, is the correlative of the latter part of the
episode of lake Algonquin—that part which comes after
the closing of its Trent Valley outlet, supposing the
lake to have drained for a time in that direction.
2. The place of the sudden contraction of the gorge at
the upper side of the Eddy basin is the correlative of
the breaking of the ice-dam in the Ottawa valley and the
opening of northeastward drainage—the end of Lake
Algonquin.
3. The episode of the gorge of the Whirlpool rapids is
the correlative of the episode of Nlpssing Great Lake
with the Niplssing-Mattawa River at its outlet—
episode of the Champlaln marine submergence.
4. The place of expansion at the lower end of the Upper
Great Gorge above the railroad bridges is the correlative
of the change of outlet of the upper lakes from North Bay
to Port Huron—the beginning of the Champlaln uplift.
5. The episode of the Upper Great Gorge is the correla-
tive of the modern of post-champlain episode of the upper
Great Lakes.
381. Taylor, Prank B. 1926. Evidence of recurrent depression
and resilience in the region of the Great Lakes.
Papers of the Michigan Academy of Science, Arts and
Letters. 7: 135-1^3.
On theoretical grounds depression and resilience of the
land in the Great Lakes region have occurred in connec-
tion with at least the last three of the Pleistocene ice
sheets. Evidence used is that of the successive Niagara
gorges - the gorge of the Wisconsin Niagara (now in the
making); the gorge of the Illinoian Niagara (the buried
St. David's gorge, and the gorge of the Kansan Niagara)
-------
(Spencer's Erigan Canyon). Included is a sketch map of
part of the Niagara Peninsula between Lakes Erie and
Ontario showing the location of the Niagara escarpment
and the three gorges described In the text.
382. Taylor, P. A. 1969. Numerical models of airflow above
Lake Ontario. September 1, 1968 and May 31, 1969.
(Final Report on IFYGL sponsored research. Research
sponsored by Meteorological Branch), Univ. of
Torontos Department of Mathematics. 65 p.
A numerical model of airflow in the lowest 50-100 m of
the atmosphere above changes In surface roughness and
temperature or heat flux has been developed based on
boundary layer approximations, the Businger-Dyer hypo-
theses for the non-dlmenslonal wind shear and heat flux
and a mixing-length hypothesis.
Results have been obtained from several situations, in
particular, airflow with neutral upstream conditions
encountering a step change in surface temperature or heat
flux with no roughness change. In these cases large
increases in shear stress at the outer edge of the
internal boundary layer are predicted. The case of
unstable upstream flow encountering a step change to
zero heat flux is also considered.
Finally, two situations thay may be encountered near the
shores of the Great Lakes are considered. Results are
presented using typical values of roughness, temperature,
etc. for cases of cold air advectlon off the land onto a
lake in winter and the lake breeze in summer. Recommen-
dations are made regarding the IFYGL observational
programme. (Canada Centre for Inland Waters).
Terasmae, J. - See: G. D. Hobson, No. 207, 208.
Terasmae, J. - See: P. F. Karrow, No. 228.
383. Thomas, J. F. J. 195^. Industrial water resources of
Canada water survey report No. 3> Upper St. Lawrence
River-Central Great Lakes Drainage Basin in Canada.
Canada Department Mines and Technical Surveys,
Mines Branch, Ottawa. 212 p.
Tabulated data for the surface water of Lake Ontario are
presented on: water temperature, water levels, specific
conductance, turbidity, suspended matter, color and dis-
charge. Descriptive statements are included which give
date and location of sampling and depth of sampling.
(Canada Centre for Inland Waters).
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3814. Thomas, M. K. 1953. Climatological atlas of Canada.
National Research Council, Ottawa. No. 3151, 255 p.
Included in this comprehensive climatological report are
the following parameters pertaining to the Lake Ontario
region.
1, Temperature - seasonal variations,
2. Humidity.
3. Wind - mean velocity and direction.
4. Snow.
5. Precipitation.
6. Radiation and cloud cover.
7. Seismological disturbance.
(Univ. of Toronto, Zoological Library)
385- Thomas, M. K. 1964. A survey of Great Lakes snowfall.
Proceedings 7th Conference, Great Lakes Research
Division, Univ. of Michigan. Publication 11.
pp. 29^-310.
Survey results of snow measurement on Lake Ontario date
back to 1842, Snowfall in the Great Lakes basin is
produced by both large scale cyclonic storms and by the
relatively small lake effect storms. Lake effect storms
seem to have greater yearly and decade to decade
fluctuations.
Thomas, M. K. and S. R. Anderson. 1967. Guide to the
climatic maps of Canada. Department of Transport,
Meteorological Branch, Toronto. 107 p.
This article provides an explanation of parameters mapped,
a subject and publication guide, and an index of important
maps published. It is designed to reduce the effort in
locating and abstracting various climatic maps of Canada.
Accompanied with the article are several climatic maps
on temperature, precipitation and barometric pressure
along with their seasonal variations. (Univ. of Toronto,
Zoology Library).
Thomas, R. L. - See: P. S. Cronan, No. 134.
Thomas, R. L. 1969a. A note on the relationship of
grain size, clay content, quartz and organic carbon
in some Lake Erie and Lake Ontario sediments.
Journal of Sedimentary Petrology. 39(2): 803-809-
An examination of the geochemistry of fine grade sediments
l;i relation to size frequency distribution was carried out
on sediment samples from Lakes Erie and Ontario. This
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study demonstrated a direct relationship between the
2 micron grain size and the theoretical clay content
computed from the organic carbon, quartz and carbonate
content. A sympathetic relationship was observed between
clay content and organic carbon, and also between grain
size and quartz content. The former relationship is
believed to be the result of absorption from solution and
the latter is brought about by natural sedimentation from
suspension.
388. Thomas, R. L. 1969b. The qualitative distribution of
feldspars in surficial bottom sediments from Lake
Ontario. Proceedings 12th Conference Great Lakes
Research, pp. 364-379.
A qualitative assessment of the feldspar distribution in
Lake Ontario sediments has been made by the determination
of the feldspar end members, K, Na and Ca, on sediment
residues after fusion with potassium pyrosulphate. Both
K absorption and cation exchange of Na and Ca for K in
standard feldspars was observed. Cation exchange is
shown to be minimal in samples and in standards with a
full particle size range. K absorption is high yet
appears to be constant and not directly related to grain
size. In the inshore zones a poor positive correlation
of feldspar to quartz is believed to be the result of
poor mixing in the traction load sediment. In the basin
zones3 the relationship is of a higher order and reflects
natural sorting by sedimentation from a suspended load.
The regional distribution of the feldspars shows an in-
shore to offshore decrease, initially, of calcic feldspar,
then of sodic feldspar leading to a basin enrichment of
the potash feldspars, microcline and orthoclase. The
feldspars are probably derived predominantly by coast
line erosion of galcial deposits surrounding Lake Ontario.
389. Thomas, R. L., A. L. W. Kemp and C. P. M. Lewis. 1970.
The distribution and characteristics of Lake Ontario
surface sediments. Abstract of paper presented at
Annual Meeting Geological Society of America, p.
703.
By use of grab samples and bottom echo sounding, the
following parameters were measured: Sediment particle
size, pH, E.H., organic carbon, carbonate carbon, quartz
content and mineral clay.
Three basin areas were recorded:
1. Nearshore - glacial meterial.
2. Offshore - covered clays deposited in Lake Iroquois.
3. "Further Offshore" - silty clays.
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The modern sediments of the lake prograde offshore into
deeper waters of each depositional basin. From inshore
to offshore, a decrease in mean grain size is associated
with a decrease in quartz and an increase in organic
carbon and clay content. Carbonate compounds are derived
from weathering limestone in the bottom areas.
390. Thompson, J. H. 1966. The geography of New York.
Syracuse University Press, Syracuse, N. Y. 53 p.
The geography of New York State is discussed in relation
to lakes s rivers, topography,, geographical features,
mountain formations, glacial developments and deposits.
391. Touvell, W. M. 1965. The Niagara River escarpment.
Royal Ontario Museum, Uriiv. of Toronto. 16 p.
The "What, why, when, how, where and who" of the
existence and formation of the Niagara Escarpment. Along
with a discussion of the geology of the area, the author
Inlcudes the process of formation of the Niagara Escarp-
ment along with the subsequent formation and erosion of
Niagara Palls. (Canada Centre for Inland Waters).
392. Touvell, W. M. 1966. Niagara Palls, story of a river.
Royal Ontario Museum, Univ. of Toronto. 16 p.
The "What, why, when, how, where and who" answers about
the formation and existence of Niagara Palls. The author
follows the process of Geological formation and erosion
along with an indepth discussion of the geology of the
area in reference to velocity of erosion. (Canada
Centre for Inland Waters).
Towle, E. L. - See: R. G. Sutton, No. 375.
Traversy5 W. - See: V. K. Chawla, No. 100.
393. U. S. Congressional House Committee on Foreign Affairs.
191**. Diversion of water from the Great Lakes and
Niagara River. 63d Congress, 2d Session. Vol. 1.
A discussion of the use of additional water from the
Niagara River for power utilization. Involves legal
aspects, effects on water levels in the river and
associated lakes and river shore ownership and utiliza-
tion policies. Several papers are included in one volume
which represents the stated opinions of various experts
and dignitaries.
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394. U. S. Department of Interior. 1963. Water levels of the
Great Lakes. Fish and Wildlife Serivce. 60 p.
The current Corps' plan to regulate the levels of the
Great Lakes (Plan 57-EO-l of Plan G) will affect only Lake
Erie. A test of this regulation plan over a 91-year
period of record revealed that the maximum mean level at
Lake Erie (573.71) would have been 1.03 feet below the
recorded adjusted level, and that the minimum mean level
(570.51) would have been 0.68 feet above the recorded
adjusted level, an average range of stage of 3.20 feet.
In other words, the plan will moderate the fluctuations of
the lake by reducing the high levels and by raising the
low levels. The highs usually occur between May and July,
and the lows are in December and January.
No evidence has been found which would indicate that this
plan will have any marked effect on the fishery resources
of Lake Erie.
The principal wildlife resources of Lake Erie are in the
form of extensive marshes which provide valuable waterfowl
and fur-animal habitat. Due to the gradual gradient at
the weatern end of the lake, water level fluctuations can
affect large acreages of these marshes. Fluctuations are
cuased by seiches, as well as by seasonal changes in the
lake level.
Most of these marshes are developed as wildlife habitat by
either public agencies or private hunting clubs. Develop-
ment is primarily in the form of dikes, water control
structures and pumps which permit control of water levels
in the marshes independent of lake levels. However, high
lake levels coupled with strong winds can be damaging to
these developments and maintenance costs are high. The
Corps' regulation plan will help to reduce these high
levels and thus alleviate the maintenance problem.
Although high lake levels may be undesirable inso far as
controlled marsh areas are concerned, they may be bene-
ficial in their effects on uncontrolled marsh areas.
High levels enhance the quality of these marshes by
creating openings in solid stands of emergent marsh
vegetation. However, most marsh areas are now under
control so this beneficial aspect of high levels is
limited to the few remaining uncontrolled areas.
In conclusion, it may be stated that the overall effects
of the Corps' regulation Plan 57-EO-l will be beneficial
-169-
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to wildlife resources of the Lake Erie area. So far as
it can be determined at this time, the plan will not
change the fishery resources of Lake Erie. (Canada
Centre for Inland Waters).
395. U. S. Department of Interior. 1965. Water resources data
for New York, surface water records. Geological
Survey. Parts 1 and 2. 378 p. and 112 p, respec-
tively.
This paper contains extensive depth and discharge data
for Lake Ontario tributaries. Information is presented
on data collection, processing methods and equipment
(gauging stations). The stations reveal seasonal,
monthly and daily discharge variation. Information is
given in part two about ground water, precipitation,
water temperature and sedimentation.
396. U. S. Department of Interior. 1966a. Statement on water
pollution in the Lake Ontario basin. Federal Water
Pollution Control Administration, Great Lakes Region,
Chicago, Illinois. 48 p.
The sources, amounts and effects of pollutants in the Lake
Ontario Basin. Each major tributary, inflow and outflow
is isolated and analyzed for flow volume, runoff, pollu-
tants, demographic data, temperature, geology, water uses
and recreation. All data is then tied together to give
an all-over picture of the situation in the Lake Ontario
basin.
397. U. S. Department of Interior. 1966b. Water resources
data for New York, surface water records. Geological
Survey. Parts 1 and 2, 363 p and 167 p, respectively.
This paper contains extensive depth and discharge data for
Lake Ontario tributaries. Information is presented on
data collection, processing methods and equipment (gaug-
ing stations). The stations reveal seasonal, monthly and
daily discharge variation. Information is presented In
part two about ground water, precipitation, water tempera-
ture and sedimentation.
398. U. S. Department of Interior. 1967a. Water oriented
outdoor recreation in the Lake Ontario basin. Bureau
of Outdoor Recreation, Ann Arbor, Michigan. 108 p.
This article contains extensive data on physical and
dimensional parameters of Lake Ontario. The location,
climate, land features, water characteristics (lake
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levels, currents, seiches), land and water uses, water
supply and pollution are all discussed in this article.
(Canada Centre for Inland Waters).
399. U. S. Department of Interior. 1967b. Water Resources
data for New York, surface water records. Geological
Survey. Parts 1 and 2, 375 p. and 159 p., respec-
tively.
This paper contains extensive depth and discharge data
for Lake Ontario tributaries. Information is presented
on data collection, processing methods and equipment
(gauging stations). The stations reveal seasonal,
monthly and daily discharge variation. Information is
given in part two about ground water, precipitation,
water temperature and sedimentation.
This paper contains extensive depth and discharge data
for Lake Ontario tributaries. Information is presented
on data collection, processing methods and equipment
(gauging stations). The stations reveal seasonal,
monthly and daily discharge variation. Information is
given in part two about ground water, precipitation,
water temperature and sedimentation.
400. U. S. Department of Interior. 1968. Water Resources
data for New York, surface water records. Geological
Survey, Parts 1 and 2. 300 p. and 137 p., respec-
tively.
This paper contains extensive depth and discharge data
for Lake Ontario tributaries. Information is presented
on data collection, processing methods and equipment
(gauging stations). The stations reveal seasonal,
monthly and daily discharge variation. Information is
given in part two about ground water, precipitation,
water temperature and sedimentation.
U. S. Department of Interior. 1969. Water Resources data
for New York, surface water records. Geological
Survey, Parts 1 and 2. 283 p. and 119 p., respec-
tively.
This paper contains extensive data on discharge and
tributary depth of rivers flowing into Lake Ontario.
Information is presented on data collection, processing
methods and equipment (gauging stations). The stations
reveal seasonal, monthly and daily discharge variation.
Information is given in part two about ground water,
precipitation, water temperature and sedimentation.
-171-
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402. U. S. Department of Interior. 1970. Water Resources data
for New York, surface water records. Geological
Survey. 301 p.
This paper contains extensive data on discharge and depth
of tributary flow into Lake Ontario. Information is pre-
sented on data collection and processing methods and
equipment (gauging stations). The stations reveal season-
al, monthly and daily discharge variation.
403. U. S. Fish and Wildlife Service. 1969. Fish and Wild-
life as related to water quality of the Lake Ontario
basin. Fish and Wildlife Service, Washington, D. C.
128 p.
Included in this report is a discussion of the morphometry,
thermal conditions, light penetration, transparency and
currents of the Lake Ontario basin. Pollution in the
various subbasins (Niagara River, Genesee River, Oswego
River, Black River and St. Lawrence River) is also
discussed.
404. U. S. Geological Survey. 1948. Ground water supply of
the United States - 1948. Geological Survey Water
Supply Paper 1114. U. S. Government Printing Office,
Washington, D. C. Part 4. 296 p.
Extensive data is presented on ground water levels
throughout the United States. The report is broken into
small areas (cities, counties, etc.) and into yearly
analysis to give accurate analyses of level fluctuations.
Very little discussion accompanies the data.
405, U. S. Geological Survey. 1952. Ground water supply of
the United States - 1950. Geological Survey Water
Supply Paper 1174. U. S. Government Printing Office,
Washington, D. C. Part 4. 309 p.
Extensive data is presented on ground water levels
throughout the Northeastern United States. The report is
broken into small areas (cities, counties, etc.) and into
yearly analysis to give accurate analyses of level fluc-
tuation. Very little discussion accompanies the data.
406. U. S. Geological Survey. 1958. Compilation of records
of surface waters of the U. S. through September,
1950. Geological Survey Water Supply Paper 1307.
397 p.
-172-
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The data presented comprise a description of gauging
stations in St. Lawrence and Lake Ontario tributaries,
tables of monthly and yearly discharge and runoff. The
station location is presented, the tributary drainage
area, mean and extremes of discharge.
407. U. S. Geological Survey. 196?a. Surface water records
of New York 1962. U. S. Geological Survey, Water
Resources Division, Albany, N. Y. 355 p.
The surface water records for the 1962 water year for
gauging stations, partial-record stations and miscellane-
ous sites within the State of New York are given in this
report. Tabulated data on daily water discharge in cfs
for streams tributary to Lake Ontario and St. Lawrence
River including the Niagara, Genesee, Black and Oswego
Rivers. Descriptive statements are included for each
sampling station. Included in these statements are
sampling location, area (in sq. miles) of drainage,
records available, average discharge, extremes and
remarks.
408. U. S. Geological Survey. 196?b. Surface water records
of New York 1963. U. S. Geological Survey, Water
Resources Division, Albany, N. Y. 369 p.
The surface water records for the 1963 water year for
gauging stations, partial-record stations and miscellane-
ous sites within the State of New York are given in this
report. Tabulated data on da-^ly water discharge in cfs
for streams tributary to Lake Ontario and St. Lawrence
River including the Niagara, Genesee, Black and Oswego
Rivers. Descriptive statements are included for each
sampling station. Included in these statements are
sampling location, area (In sq. miles) of drainage,
records available, average discharge, extremes and
remarks.
409. U. S. Geological Survey. 196?c. Surface water records
of New York 1964. U. S. Geological Survey, Water
Resources Division, Albany, N. Y. 362 p.
The surface water records for the 1964 water year for
gauging stations, parti3i.-record stations and miscellane-
ous sites within the State of New York are given in this
report. Tabulated data on daily water discharge In cfs
for streams tributary to Lake Ontario and St. Lawrence
River including the Niagara, Genesee, Black and Oswego
Rivers. Descriptive statements are Included for each
sampling station. Included in these statements are
sampling location, area (in sq. miles) of drainage,
records available, average discharge, extremes and
remarks.
-173-
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410. r;. s. Geological Survey. 1961. Surface water supply of
the United States. Part 4 - St. Lawrence River
basin, I960. Geological Survey Water Supply Paper
1707, 437 p.
Extensive data is presented on the surface water supply
in the St. Lawrence River basin. The report is broken
into small areas (cities, counties, etc.) and into yearly
analysis to give accurate analyses of level fluctuation.
Very Little discussion accompanies the data.
'411. U S, leclorlcal Survey. 1964a. Compilation of records
of surface waters of the U. S., October 1950 to
September I960. Part 4 - St. Lawrence River basin.
'/. S, Geological Survey Water Supply Paper 1727-
379 p.
Runoff and discharge parameters for all major rivers
running Into and out of Lake Ontario, including the
Niagara River inflow and the St. Lawrence outflow. The
location and drainage area of each river Is also listed.
(Canada Centre for Inland Waters).
4]2. V 3. Geological Survey. 1964b. Ohio River basin and
St. Lawrence River basin. Water Supply Paper No.
1935. ;->4o p.
Tabulated surface water data Include:
Temperature Sediment composition
Water color Station equipment and location
Strearn aischarge
The samples were taken at gauging stations throughout
the lake and various tributaries.
413. U. S, Geological Survey. 1965a. Ground water levels
In the United States - 1958-62. Geological Survey
Watfi.o Supply Paper 1782. U. S. Government Printing
OfMr;-, Washington, D. C. 252 p.
Extensive data Is presented on ground water levels
throughout the Northeastern States. The report is broken
into small areas (cities, counties, etc.) and into yearly
analysis to p;Ive accurate analyses of level fluctuations.
Very little discussion accompanies the data.
414. l.i, S. Geological Survey. 1965b. Magnitude and frequency
of flood? in the U. S. - Part 4. The St. Lawrence
River Easln, U. S. Geological Survey, Water Supply
•Paper l6?7. 357 p.
-174-
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Data is presented on discharge runoff, and related flood
levels for all major rivers running into Lake Ontario and
the St. Lawrence River. Data is also presented on river
location and drainage area. (Canada Centre for Inland
Waters).
U. S. Geological Survey. 1968. Water resources inves-
tigations in New York. Water Resources Commission,
Albany, M. Y. Unnumbered.
Tables, maps and a bibliography of various essential
components to a general understanding of the quality,
quantity and composition of the water resources of New
York State. Included are information on drainage, tem-
perature, discharge and geology of New York State per-
taining to water quality, quantity and composition.
U. S. Geological Survey. 1969. Quality of surface waters
of the United States - 1964. Geological Survey Water
Supply Paper 1955- U. S. Government Printing Office,
Washington, D. C. Parts 3 and 4. 440 p.
The article encompasses many physical and chemical para-
meters pertaining to pollution levels and x^ater quality
in the St. Lawrence Basin. The major physical parameters
are: mineral constituents of water, specific conductance,
color, temperature, turbidity and sediment.
417. Upchurch, S. B. 1970a. Great Lakes basin - Limnology of
lakes and embayments. Great Lakes Basin Commission,
Ann Arbor, Michigan. 37 p.
Parameters Included are; location, geology, dimensions,
climate, winds and storms, temperatures, precipitation,
runoff and groundwater. The interrelationship of many
of these parameters are discussed in reference to climate
and physical characteristics of the Lake.
4l8. Upchurch, S. B. 1970b. Lake basin physiography -
Limnology of lakes and embayments, Great Lakes Basin
Commission, Ann Arbor, Michigan. 23 p.
The paper includes in depth discussion on the drainage
characteristics of the Lake Ontario and the tributaries
leading to the Lake. The discussion includes several
important drainage parameters. These parameters Include:
Drainage volume and areas Dimensions
Runoff Locations
Lake level
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419. Upham, W. 1896. Origin and age of the Lawrentian Lakes
and of Niagara Falls. American Geologist. 28: 169-
17?.
The article discusses the preglacial condition of the
St. Lawrence basin, changes bringing; on the ice age,
recessions of the ice sheet, glacial lakes in the St.
Lawrence basin (Warren, Algonquin and Iroquois), the
beginning of ths Niagara River and Its erosion of the
gorge below the falls, flow variation in the Niagara
River, duration of Niagara Palls of the postglacial
period.
420. Upham, W. 1898. Niagara Gorge and St. David's Channel.
Bulletin of Geological Society of America. 9' 101-
110.
The report contains Information on:
1. The Niagara Gorge - physical features.
2. St. David's Channel - preglacial extent, effects on
the recession of the falls and location.
3. The effect of the Lawrentlal Lakes on the Niagara
Gorge erosion.
4. Epeirogenic uplifting continued to the present time.
5. Epeirogenic uplifting contemporaneous with the
glacial lakes»
6. Duration of Niagara Palls and the postglacial period.
421. Vanderpast. J. M. and B. J. Dutka. 1970. A bacterio-
logical study of sediments in the Kingston basin and
Lake Ontario outlet of the St. Lawrence River.
Manuscript Report No. KR. 70-3. Division of Public
health Engineering, Department of National Health
and Welfare, Ottawa. 110 p.
During July, 1970, a detailed sediment sampling program
was undertaken in the Kingston Basin and the St. Lawrence
River outlet of Lake Ontario, by the LImnogeology Section
of the Canada Centre for Inland Waters. Since there was
no record of any bacteriological studies of the sediments
in this area, a program, of sediment analysis, designed to
present detailed bacteriological Information about the
outflow environment of Lake Ontario was Initiated.
Specifically, the area lies between 44°04'N and *U°l6'N
and 76°20'W and 76°47'W. Prom this study, it was anti-
cipated that distribution patterns of bacterial densities
and bacterial blotypes for the study area would be
obtained. An investigation Into the effect, if any, of
local conditions, ie. sewage treatment plant discharge
-17b-
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industrial wastes, streams, on bacterial densities and
biotype distribution, was also planned.
Prom the CCIW Vessel Lemoyne, sediment samples were
collected by means of a Shipek grab sampler. Prom these
Shipek samples, cores were removed by means of sterile
plastic cylinder and the 0-2 and 4-6 cm sediment layers
were tested for the following bacteriological parameters:
coliform MF, 20°C MP plate count; 20°C MP anaerobic plate
count; sulfate-reducing bacteria MPN; and autotrophic
ammonium-oxidizing bacteria MF.
Twenty-two gram portions of sediment were belnded with
198 ml of phosphate buffer, at low speeds for one minute.
Prom this blended sample, allquoits were Immediately
tested for the various parameters.
Collforms were found only in a few samples, in three
widely dispersed areas. The highest coliform density
recorded was 1200 coliforms per gm dry wt.
Aerobic bacterial densities were lowest in shallow rocky
or sandy areas and Increased as the sediments graded to
black silt in the deeper basins. In the majority of
samples the highest aerobic bacterial densities were
found in the 0-2 cm layer with densities ranging from
80,000 per gm dry wt. in gravel or glaciolacustrine
clay to 57,000,000 per gm dry wt, in black silty muds.
Anaerobic plate count densities were much lower than
aerobic plate count densities. In two-thirds of the
samples, higher anaerobic densities were found in the 0-2
cm layer than in the 4-6 layer.
Sulfate-reducing bacterial densities correlated very
closely with anaerobic plate count densities, with the
highest densities also occurring in the 0-2 cm sediment
layer. A definite correlation between high sulfate-
reducing bacterial densities, water depth and sediment
type, i.e. black silty muds, was observed. Nitrifying
bacteria were only found sporadically and their isola-
tion appeared to correlate with industrial sites, farm-
Ing ar-eas and population densities.
422. Verber, J. L. 1966. Inertial currents in the Great
Lakes. Great Lakes-Illinois River basin project,
PWPCA. Proceedings Great Lakes Research Division,
Univ. of Michigan. Publication 15, pp. 375-379.
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The Great Lakes Illinois River Basins Project has
completed field studies on currents on Lakes Michigan,
Erie and Ontario. One of the dominant effects appears to
be that the earths rotation produces right hand accelera-
tion to the currents. The effects of the earths rotation
on water movements In the Great Lakes has been portrayed
in a film. Five patterns of flow are displayed: straight
line flow, sinusoidal or oscillatory, half moon, circular
or spiral and rotary or screw. Inertial flow is found in
the Great Lakes at all depths and in all seasons, as well
as under ice cover. With few exceptions, such as in the
Straits of Mackinac and shallow Inshore stations, some
type of Inertial flow is evident in the lakes.
423. Watt, A. K. 1951. Ground water in Ontario - 1947.
Ontario Department of Mines. 60(11): 1-116.
Report contains extensive geological information, as well
as topographic information of the Province of Ontario.
A great deal of data are presented in Lake Ontario
elevation, water levels and effects of runoff on water
quantity and quality. (Univ. of Toronto, Great Lakes
Institute).
424. Watt, A. K. 1961. Ground water in Ontario - 1953-54.
Ontario Water Resources Commission, ground-water.
Bulletin No. 1. 320 p.
This report contains data on Ontario ground water along
with the geography, geology, drainage and climate of the
province. Data are presented on Lake Ontario elevation,
levels, runoff, water quality and quantity. (GLIK
425- Watt, A. K. 1963. Ground water in Ontario - 1955-56.
Ontario Water Resources Commission, Ground Water.
Bulletin No. 2. 377 p.
This report contains data on Ontario ground water along
with the geography, geology, drainage and climate of the
province. Data are presented on Lake Ontario elevation,
water levels, runoff, water quantity and quality.
(Univ. of Toronto, Great Lakes Institute).
426. Watt, A. K. 1965. Ground water in Ontario - 1957.
Ontario Water Resources Commission, Ground Water.
Bulletin No. 3. 206 p.
This report contains data on Ontario ground water along
with the geography, geology, drainage and climate of the
province. Data are presented on Lake Ontario elevation,
water levels, runoff., water quality and quantity.
(Univ. of Toronto,, Great Lakes Institute).
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427. Watt, A. K. 1966. Ground water in Ontario - 1958.
Ontario Water Resources Commission, Ground Water.
Bulletin No. 4. 257 p.
This report contains data on Ontario ground water along
with the geography, geology, drainage and climate of
the province. Data are presented on Lake Ontario eleva-
tion, water levels, runoff, water quantity and quality.
(Univ. of Toronto, Great Lakes Institute).
428. Webb, M. S. 1970. Monthly mean surface temperatures for
Lake Ontario as determined by aerial survey. Water
Resources Research. 6(3): Unnumbered.
For calculations of evaporation losses by mass transfer
techniques, and for many other research and operational
applications, it is necessary to know the mean patterns
of surface water temperature. The work of Millar (1952)
has been widely used whenever such information is
required for the Great Lakes. This paper presents pre-
liminary patterns of monthly mean surface water tempera-
tures for Lake Ontario based on 36 airborne radiation
thermometer surveys over a three-year period. Tempera-
ture values at each of the 89 points in a grid have been
plotted against calendar date, and an annual temperature
curve has been produced for each point. Values for the
middle of each month have been determined by interpola-
tion, and used to produce a pattern for each month.
The patterns are briefly compared with Millar's. Over
the next few years as the airborne radiation thermometer
(ART) surveys continue to add to the data band, it is
planned to update these analyses. Therefore, these
monthly values must be considered tentative at this
time. (Canada Centre for Inland Waters).
429. Weiler, H. S. 1968. Current measurements In Lake
Ontario in 1967. Proceedings llth Conference Great
Lakes Research, pp. 500-511.
During the summer of 1967, two sets of moorings with
current meters were placed in Lake Ontario, by the
Canada Centre for Inland Waters. Data sampling was
every 10 minutes, and the data from temperature, water
speed and direction sensors was recorded in 1/4 inch
magnetic tape. Initial analysis has begun, and pre-
liminary results show that during summer stratification,
there are edge waves traveling counter-clockwise along
the northern shore near Toronto, which have a phase
speed of less than half that determined from theoretical
consideration. The difference for the 17 hour periodi-
city Is not considered significant, since the actual
•179-
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configuration of the bottom or stratification does not
conform to the theoretical models.
430. Weiler, H. S. and C. R, Murthy. 1971. The Niagara
River plume, Part 1., temperature and current
structure in the Niagara River plume; Part 2, the
mixing of the Niagara River plume in Lake Ontario.
Inland Waters Branch,, Technical Bulletin No. 38,
Canada Centre for Inland Waters. Unnumbered.
A descriptive study off the mouth of the Niagara River
was carried out in 1968 to obtain information on the
dynamic behaviour of the river's plume, both in terms
of gross movement, as well as diffusive properties.
Part 1 of the report encompasses the results of tempera-
ture surveys, drogue tracking experiments and infrared
line scanner mosaics. These results show that the
river's plume Is strongly influenced by the dominant
winds of the day before the experiment, ar)d to a lesser
extent those of the preceding day. Response time of the
plume to persistent changes In wind was estimated to be
between 1 and 2 days. Surface currents in the lake,
driven by over-lake winds, controlled the motion of the
plume; the motion t^as quite varied and complex, depend-
ing on the wind fields encountered, a fact that showed
up most clearly on the Infrared line scanner mosaics.
Part II of the report encompasses the diffusion studies
carried out in the same area. The mixing of the river's
plume with the main body of the lakes was found to take
place intwo stages. Fairly close to the river's mouth,
very strong river-type mixing was found. Beyond this
area, buoyant surface spread of the warmer river water
over the colder lake water occurred. These findings are
consistent with the results of Part I. (Canada Centre
for Inland Waters).
Weist, W. G. and G. L. Giese, Water resources of the
central New York region. U. S. Geological Survey,
Albany, N.Y. Bulletin No. 64. 58 p.
This report summarized the available data on the water
resources of the Central New York Region which includes
Cayuga, Cortland, Madison, Onondaga and Oswego Counties---
an area of 3,622 square wiles centering around Syracuse.
The 7^0,000 people living in the region use about 310 mgd
(million gallons per day) of water for domestic and indus-
trial purposes. About 90% of this water presently comes
from surface-water sources.
•179-b
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The region Includes parts of four major drainage basins:
the Mohawk River, the Oswego River, the Susquehanna
River and the Lake Ontario plains. Streamflow in the
region is highly variable both from time to time, and
from place to place. Generally, flow is greatest during
March through May and lowest during July through Septem-
ber. During periods of low flow, most of the vrater comes
from ground-water discharge. Streams such as Chittenango
Creek, that have large areas of storage in lakes, swamps,
or extensive permeable deposits along them, have larger
more dependable low flows than do streams that lack such
storage areas. These streams may even go dry during
periods of deficient rainfall. The only stream with a
minimum average 7-day. 2-year flow greater than 50 cfs
(cubic feet persecond) are the Salmon River below Salmon
River Reservoir and the Seneca, Oneida and Oswego Rivers.
Over half of the streams in the region have a minimum
average 7-day, 2-year flow less than 2 cfs. In general,
the quality of the surface water tends to be better than
than of most of the flow which comes from the ground
water.
Ground water in the region occurs in both consolidated
deposits (bedrock) and unconsolidated deposits (sand,
gravel, etc.). The bedrock can be divided into seven
units on the basis of similarity of llthology and
hydrologic properties. These units are, in ascending
order from north to south: lower shale, sandstone,
sandstone-shale, dolomite, middle shale, limestone and
upper shale. In all of these units, ground water occurs
chiefly along bedding planes and joints. In the more
soluble units, such as the limestone and middle shale,
these openings have been enlarged by solution. The
middle shale unit contains considerable amounts of gypsurn
and salt, which are soluble in water; thus its water is
almost invariably of very poor quality. Water from the
limestone is likely to be very hard, but usable v.'hereas
water from the remaining bedrock units is generally of
better quality.
The best source of ground water In the region are the un-
consolidated deposits of sand and gravel in the major
valleys. The amount of water available from these
deposits commonly can be increased through induced
recharge or artificial recharge. A total of more than
240 mgd can be developed from the better sand and gravel
aquifers. Water from the unconsolidated deposits
generally reflects the quality of the water of the under-
lying bedrock.
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^32. Whittlesey, C. 1867. On the ico movement of the glacial
era in the valley of the St. Lavrrenoe, Proceedings
American Association Advancement of Science, 15th
Meeting, pp. 43--51*.
Extensive analysis of glacial depoc-f.tr-, their location,
occurrence, properties and structures ^s UH^ to analyse
the extent, numbers and movements of the various Ice
sheets in the St. Lawrence Vallev.
^33. Wiggln, B. L. 1950. Great snors of the Great Lakes.
Weatherwise. 3(6); 123-12*.
Citing the great snow storms which haw occurred In the
area in the past, several conclusions "bout lake effect
storms are reached. They are prevalent when: 1) cold
polar air moves across the lake^ 2) there is a cyclonic
curvature to the flow pattern, 3) liter* 1;; i definite
air water temperature difference, Ji > t,;;ere *s a long
fetch over the water and 5) there Lr .? shear" -:o produce
longilu convective cells.
The worst storm occurring was in Janunry of 194? with 8*
of snow and 20* drifts occurring..
4 3^. Williams, E. T. 1916. Niagara-queen of wonders.
Chappie Publishing Company,, Ltd,., Boston, 188 p.
A graphic history of the big events in three centuries
along the Niagara Frontier, one of the most famous
regions in the world, including ear;v explorations, early
literature, early wars, electrical newer development,
area conservation of natural rasourcos and oreation and
development of the City of Niagara Falls. fErhoellkopf
Museum, Niagara Palls, M. Y.)«
Williams, G. W. - See: P. E. Greeson, ?Io. 19?.
435. Wilshaw, R. and D. R. Rondy. 1965. Orost .la'/v* ice
cover, winter 196^-65. Lake Survey, Oorr ^ of
Engineers, Detroit, Michigan. Report 5-1, ?6 p.
In January of 1963, the U. S. Lake Survey inj t,J &lea a
program to acquire data related to the formation, distr-j-
bution, movement and decay of ice in the Gre^t Laker,
Data were collected at predetermine! time intervalo c.t
selected locations by utilizing aerial photoj-rspby and
visual observations. This reporc covers tn^ r;eocedures
and methods used for collecting Ice cover da^.a •sn the
Great Lakes for the winter of 196'4~65. (Canada Centre
for Inland Waters).
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Woodrow, D. L. - See: R. G. Sutton, No. 373.
436. Woodrow, D. L., R. G. Sutton and N. A. Rukavina. 1967.
A drowned beach in Lake Ontario, west of Rochester,
New York. Proceedings 10th Conference Great Lakes
Research, pp. 157-161.
Fathometer traces, cores and grab samples were utilized
to determine the configuration of the bottom and the
distribution of the bottom sediments in nearshore Lake
Ontario between Rochester and Braddock Point New York.
The data indicate a smooth, sandy bottom extending from
the present shoreline to water depth of 25 feet. A
rough, steep sloping bottom with boulder accumulations
exists between water depths 25 and 50 feet. At water
depths greater than 50 feet, the bottom is smooth and
silty. The boulder size zone is parallel to the modern
shoreline and is approximately 1/2 mile offshore. The
writers interpret the boulder zone as a drowned beach.
The bays and swamp landward of the drowned beach have
been covered by modern lake sediments.
437. Wright, G. F. 1898. The age of Niagara Falls as
indicated by the erosion at the mouth of the gorge.
Abstract of paper presented American Association
Advancement of Science, 47th Meeting, pp. 299-300.
A conservative estimate of the rate of disintegration for
the 70 ft. of Niagara shales supporting the Niagara lime-
stone would be 1/5 of an inch per year, with a probable
rate of 1/2 inch per year. But at the lowest estimate
no more than 10,000 years would be required for the
enlargement of the upper part of the mouth of the gorge
388 feet on each side, which is very largely in excess
of the actual amount of enlargement. The age of the
gorge cannot be much more than 10,000 years and is
probably considerably less.
Yu, S. L. - See: W. Brutsaert, No. 46.
433. Yu, S. L. and W. Brutsaert. 1968. Estimation of near
surface water temperatures of Lake Ontario. Proceed-
ings llth Conference on Great Lakes Research, pp.
512-523.
The relationship was analyzed between Lake Ontario
surface water temperature and air temperature and sun-
shone percentage data observed at four peripheral
stations. Time series and regression analysis were
•182-
-------
performed and different estimation equations were com-
pared. It was found that there was practically no
correlation between water temperature and sunshine
anomalies, and that water temperature could be estimated
with an average coefficient of determination of 0.44 by
using the present and the past two to four months of air
temperature data.
439. Zenger, D. H. 1965. Stratigraphy of the Lockport
formation (Middle Silurian) in New York State. HY3
Museum and Science Service, Albany, N. Y. 210 p.
The origin, composition, erosion and location of the
Lockport formation in Western New York State. Atricle
includes properties and structures, material erosion and
general features. (Schoellkopf Museum, Niagara Palls,
N. Y.).
-183-
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IV. AUTHOR/AGENCY ADDRESSES
Acres, H. G.
1959 Dorchester
Niagara Palls, Ontario
CANADA
Adams, Charles C.
Roosevelt Wildlife Forest
Experiment Station
Syracuse, New York
Allen, W. T. R.
Canadian Dept. of Transport
315 Bloor Street West
Toronto 5, Ontario
CANADA
Anderson, D. V.
Department of Mathematics
University of Toronto
Toronto 5, Ontario
CANADA
Andrews, R. H. G.
801 Bay Street
Toronto, Ontario
CANADA
Archibald, D. C.
Department of Transport
Meteorological Branch
315 Bloor Street West
Toronto 5, Ontario
CANADA
Ayers, John C.
Great Lakes Research Division
University of Michigan
N. University Building
Ann Arbor, Michigan
Bakewell, R.
(Deceased)
Barrientos, C. S.
Techniques Development Lab
SDO, National Westher Ser.
NOAA
Silver Springs, Maryland
Barrows, K. K.
U. S. Geological Survey
Washington, D. C.
Beeton, A. M.
Center for Great Lakes Studies
University of Wisconsin
Milwaukee, Wisconsin 53201
Bird, S. J. G.
Dept. of Civil Engineering
University of Toronto
Toronto, Ontario
CANADA
Bolduc, P. A.
Dept. of Energy, Mines and
Resources
Ottawa, Ontario
CANADA
Bolsenga, S. J.
Great Lakes Research Center
U. S. Lake Survey
Detroit, Michigan
Bolton, E.
Geological Survey of Canada
Brebner, A.
Dept. of Civil Engineering
Queens University
Kingston, Ontario
CANADA
Broughton, J. G.
NYS Museum and Science Service
Albany, New York
Browzin, B. S.
Catholic University of America
Washington, D. C.
Bruce, J. P.
Great Lakes Division
Canada Centre for Inland Waters
P. 0. Box 5050
86? Lakeshore Road
Burlington, Ontario
CANADA
-18H-
-------
Brunk, I. W.
U. S. Weather Bureau
Chicago, Illinois
Brutsaert, W.
School of Civil Engineering
Cornell University
Ithaca, New York 14850
Buehler, E. G.
(Deceased)
Caley, J.P.
Geological Survey of Canada
Campbell, N. J.
Marine Sciences Branch
Dept. of Mines & Technical
Surveys
Ottawa, Ontario
CANADA
Canada Centre for Inland
Waters
P. 0. Box 5050
867 Lakeshore Road
Burlington, Ontario
CANADA
Canadian Dept. of Energy,
Mines & Resources
Ottawa, Ontario
CANADA
Canadian Dept. of Fisheries
& Forestry
Canadian Dept. of Mines &
Technical Surveys
Ottawa, Ontario
CANADA
Canadian Dept. of Northern
Af-faris & National
Resources
Ottawa, Ontario
CANADA
Canadian Dept. of Transport
315 Bloor Street West
Toronto 5, Ontario
CANADA
Canadian National Committee
Ottawa, Ontario
CANADA
Cartier, R. H. (Address
Unknown)
Chalmers, R.
(Deceased)
Chandler, D. C.
Great Lakes Research Division
University of Michigan
Ann Arbor, Michigan
Chapman, L. J.
Ontario Research Foundation
43 Queens Park
Toronto, Ontario
CANADA
Chawla, V. K.
Canada Centre for Inland Waters
P. 0. Box 5050
867 Lakeshore Road
Burlington, Ontario
CANADA
Chermack, E. E.
Department of Earth Science
State University College
Oswego, New York 13126
Clark, L. J.
(Deceased)
Claypole, E. W.
(Deceased)
Coakley, J. P.
Canada Centre for Inland Waters
P. 0. Box 5050
867 Lakeshore Road
Burlington, Ontario
CANADA
Coch, H. K.
University of Rochester
Rochester, New York
Coleman, A. P.
(Deceased)
-185-
-------
Corps of Engineers
Department of Army
Buffalo District
1776 Niagara Street
Buffalo, New York 1^207
Corps of Engineers
Department of Army
Detroit District
Detroit, Michigan
Corps of Engineers
Department of Army
North Central District
Chicago, Illinois
Corps of Engineers
Department of Army
Washington, D. C.
Cronan, D. S.
Department of Geology
University of Ottawa
Ottawa 2, Ontario
CANADA
Csandy, G. T.
University of Waterloo
Waterloo, Ontario
CANADA
Davies, J. A.
McMaster University
Department of Geography
CANADA
Day, P. C. (Address
Unknown)
Deane, R. E.
Dept. of Geological Sciences
University of Toronto
Toronto, Ontario
CANADA
DeCooks, B. G.
U. S. Lake Survey
630 Federal Building
Detroit, Michigan 48226
Deniscn3 N,
(Deceased)
Denison, P. J.
H. G. Acres, Ltd.
Niagara Palls, Ontario
CANADA
Dewey, C.
(Deceased)
Dobler, G. C.
Marine Sciences Branch
Dept. of Energy, Mines &
Resources
6l*l Booth Street
Ottawa 5, Ontario
CANADA
Dollen, B. H.
New York State Museum
Albany, New York
Donate, R. J.
National Research Council
Ottawa, Ontario
CANADA
Drake, R. L.
National Center for Atmospheric
Research
Boulder, Colorado
Drummond, A. T.
(Deceased)
Dunn, B.
NYS Dept. of Environmental Cons.
Water Resources Commission
Albany, Now York
Elder, P. C.
Canada Centre for Inland Waters
P. 0. Box 5050
867 Lakeshore Road
Burlington, Ontario
CANADA
Pairchild, H. H.
(Deceased)
Fisher, Donald W.
New York State Museum
Albany, New York
-186-
-------
Forrester, G. C.
331* Buffalo Avenue
Niagara Palls, New York
Frotin, J. P.
Meteorological Branch
Department of Transport
Toronto, Ontario
CANADA
Prlcbergs, K. S.
Toronto Harbour Commission
60 Harbour Street
Toronto 1, Ontario
CANADA
Gannon, J. E.
Center for Great Lakes
Studies
University of Wisconsin
Milwaukee, Wisconsin 53211
Gibbes, L. R.
(Deceased)
Gilbert, Bruce K.
Water Resources Commission
Albany, New York
Gillette, Tracey
New York State Museum
Albany, New York
Godin, G.
Canadian Dept. of Energy,
Mines & Resources
Ottawa, Ontario
CANADA
Grabau, A. W.
(Deceased)
Great Lakes Basin Hydrollc
and Hydrologic Data
Coordinating Committee
Ann Arbor, Michigan
Great Lakes Institute
(now)
Institute of Environmental
Sciences and Engineering
University of Toronto
Toronto l8l, Ontario
CANADA
Greeson, P. E.
U. S. Geological Survey
P. 0. Box 9*»8
Albany, New York 12201
Griswald, R. E.
NYS Dept. Environmental Cons.
50 Wolf Road
Albany, New York 12201
Gunwaldsen, R. W.
Stone and Webster Engineers
Boston, Massachusetts
Hackey, H. B.
(Address Unknown)
Haefeli, C. J.
Inland Waters Branch
Dept. of Energy, Mines &
Resources
Ottawa, Ontario
CANADA
Hall, J.
(Deceased)
Hamblin, P. F.
M19 Fourth Avenue, N. E.
Seattle, Washington
Hartnagel, C. A.
New York State Museum
Albany, New York
Hayes, G. E.
(Deceased)
Heath, R. C.
NYS Dept. of Environmental Cons
50 Wolf Road
Albany, Mew York 12201
-187-
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Herdendorf, C. E. Ill
Director, CLEAR
Ohio State University
Columbus, Ohio 43210
Heubusch, Carol A.
Buffalo Museum of Science
Humboldt Park
Buffalo, New York 14211
Hiney, R. A.
NYS Dept. Environmental
Conservation
Division of Water Resources
50 Wold Road
Albany, New York 12201
Hobson, G. D.
Dept. of Energy, Mines &
Resources
Inland Waters Branch
Ottawa, Ontario
CANADA
Holley, G. W.
(Deceased)
Holleyman, J. B.
ESSA Weather Bureau
Great Lakes-Illinois River
Basins Project
PWPCA, Region 5
Chicago, Illinois
Horton, J. H.
(Address Unknown)
Horton, R. E.
(Address Unknown)
Hough, J. L.
Department of Meteorology
& Oceanography
Great Lakes Research Div.
Institute of Science &
Technology
University of Michigan
Ann Arbor, Michigan 48104
Hyde, A. S.
Roosevelt Wildlife Forest
Experimental Station
SUNY College of Forestry
Syracuse, New York 13210
Hydro-Electric Power Commission
of Ontario
International Joint Commission
Pollution of Boundary Waters
Washington, D. C.
and
Ottawa, Ontario
CANADA
Irbe, J. G.
Meteorological Service of
Canada
Canada Department of Transport
315 Bloor Street West
Toronto 5, Ontario
CANADA
Juisto, J. E.
Atmospheric Science Research
Center
State University of New- York
1400 Washington Avenue
Albany, New York 12203
Johnson, E. C,
(Address Unknown)
Johnston, R. H.
NYS Dept. Environmental Cons.
Water Resources Commission
Albany, New York
Karrow, P. F.
Department of Earth Science
University of Waterloo
Waterloo, Ontario
CANADA
Kemp, A. L. W.
Canada Centre for Inland Waters
P. 0. Box 5050
86? Lakeshore Road
Burlington, Ontario
CANADA
-188-
-------
Kelgour, W. J.
(Address Unknown)
Kindle, E. M.
(Deceased)
Klrchgatter, D.
Canadian Dept. of Lands &
Forests
Parliament Buildings
Toronto 5, Ontario
CANADA
Klrshner, L. D.
(Address Unknown)
Klwanls Club
Stamford, Ontario
CANADA
Kramer, James R.
Department of Geology
McMaster University
Hamilton, Ontario
CANADA
or
Department of Geology
Syracuse University
Syracuse, New York 13210
Ku, L. P.
Marine Sciences Branch
Ottawa, Ontario
CANADA
Landsberg, D. R.
Polytechnic Institute
333 Jay Street
Brooklyn, New York 11201
Lane, R. K.
Canada Centre for Inland
Waters
P. 0. Box 5050
86? Lakeshore Ro-ad
Burlington, Ontario
CANADA
Langbeln, W. B.
U. S. Geological Survey
Washington, D. C.
Langford, G. B.
21 Lamport Avenue
Toronto 5, Ontario
CANADA
Lansing, L.
Atmospheric Research Center
State University of New York
Tug Hill Field Station
Boonvllle, New York
Laverett, F.
(Deceased)
Lemlre, F.
Great Lakes Institute
University of Toronto
Toronto 181, Ontario
CANADA
Lewis, C. F. M.
789 Sunset Road
Burlington, Ontario
CANADA
Lewis, J.M.
University of Chicago
Chicago, Illinois
Liu, P. C.
U. S. Lake Survey
630 Federal Building
Detroit, Michigan 48226
Luther, D. 0.
New York State Museum
Albany, New York
Mack, K.
NYS Dept. Environmental Cons,
Water Resources Commission
Albany, New York
Martin, J. 0.
(Deceased)
Matheson, D. H.
Municipal Laboratories
City Hall
Hamilton, Ontario
CANADA
-189-
-------
McAndrews, J. H.
Department of Biology
Cornell College
Mt. Ve rnon, Iowa
McComble, A. M.
Ontario Dept. Lands &
Forests
Southern Ontario Research
Station
Maple, Ontario
CANADA
McVehll, G. E.
Cornell Aeronautical Lab-
oratory, Inc.
P.O. Box 235
Buffalo, New York 1^221
Megerian, E.
U. S. Lake Survey
Army Corps of Engineers
630 Federal Building
Detroit, Michigan
Menon, A. S.
Bacteriological Laboratories
Public Health Engineering
Division
Dept. of National Health &
Welfare
Kingston, Ontario
CANADA
Millar, F. G.
(Address Unknown)
Miller, W. J.
New York State Museum
Albany, New York
Mortimer, Clifford 0.
Department of Zoology
Center for Great Lakes
Studies
University of Wisconsin
Milwaukee, Wisconsin 53201
Murphy, T. E.
U. S. Army Corps of Engineers
1776 Niagara Street
Buffalo, New York 1*1207
Murthy, C. R.
P. 0. Box 5050
Canada Centre for Inland Waters
Burlington, Ontario
CANADA
Newberry, J. S.
(Deceased)
Newland, D. H.
(Address Unknown)
New York State Atomic and
Space Development Authority
Albany, New York
New York State Department of
Health
84 Holland Avenue
Albany, New York 12208
New York State Department of
Environmental Conservation
50 Wolf Road
Albany, New York 12201
O'Connor, D. J.
Provessor of Civil Engineering
Manhattan College
New York, New York
Oliver, W. A., Jr.
(Addre s s Unknown)
Ontario Water Resources
Commission
135 St. Clair Avenue West
Toronto 7, Ontario
CANADA
Ostry, R, C.
Ontario Water Resources Comm.
135 St. Clair Avenue West
Toronto 195, Ontario
CANADA
-190-
-------
Owen, E. B.
Dept. of Energy, Mines &
Resources
Ot t awa, Ont ari o
CANADA
Pach, A. B.
Division of Meteorology
Department of Agronomy
Cornell University
Ithaca, New York 14850
Palmer, M. D.
Ontario Water Resources
Commission
96 Health Street, E.
Toronto 290, Ontario
CANADA
Paskausky, D. P.
Marine Sciences Institute
University of Connecticut
Groton, Connecticut
Pentland, R. L.
Department of Energy,
Mines & Resources
# 8 Temporary Building
Ottawa, Ontario
CANADA
Phillips, D. W.
Canadian Meteorological
Service
Toronto, Ontario
CANADA
Pincus, H. J.
Twin City Mining Research
Center
U. S. Bureau of Mines
P. 0. Box 1660
Twin City Airport
Minneapolis, Minnesota 55111
Pohlman, J.
(Deceased)
Pound, A.
(Address Unknown)
Powers, C. E.
Federal Water Quality Admin.
200 S. 35th Street
Corvallis, Oregon 97330
Prichard-Carpenter
Rochester Gas and Electric Corp
Rochester, New York
Radforth, I.
Department of Zoology
University of Toronto
Toronto, Ontario
CANADA
Rafter, G. W.
New York State Museum
Albany, New York
(Deceased)
Rainey, R. H.
805 Victor Drive
Knoxvllle, Tennessee
Rao, G. V.
St. Louis University
St. Louis, Missouri
Repp, R. D.
U. S. Army Corps of Engineers
1776 Niagara Street
Buffalo, New York 1420?
Richards, T. L.
Department of Transport
Meteorological Branch
315 Bloor Street West
Toronto 5, Ontario
CANADA
Rickard, L. V.
New York State Museum
Albany, New York
Robison, P. L.
NYS Dept. Environmental Cons.
Water Resources Commission
Albany, New York
-191-
-------
Rockivell, D. C.
6552 Glenwood North
Chicago, Illinois 60626
Rodgers, G. K.
Institute of Environmental
Science & Engineering
University of Toronto
Toronto 181, Ontario
CANADA
Rodgers, H. D.
(Deceased)
Rondy, D. R.
U. S. Army Corps of Engineers
Great Lakes Research Center
Detroit, Michigan
Rukavina, N. A.
Canada Centre for Inland
Waters
P. 0. Box 5050
86? Lakeshore Road
Burlington, Ontario
CANADA
Sanderson, M.
Department of Geography
University of Windsor
Windsor, Ontario
CANADA
Schutze, L. T.
U. S, Lake Survey
630 Federal Building
Detroit, Michigan 48226
Scott, J. T.
Earth and Atmospheric Science
State University of New York
Albany, New York 12203
Scovlll, J. T.
(Deceased)
Simons, T. J.
Canada Centre for Inland
Waters
P. 0. Box 505
Burlington, Ontario
CANADA
Simpson, R. B.
Dept. of Geological Sciences
University of Toronto
Toronto, Ontario
CANADA
Simpson, W. G.
Institute of Environmental
Sciences & Engineering
University of Toronto
Toronto l8l, Ontario
CANADA
Sisson, H. B.
(Address Unknown)
Slater, G.
New York State Museum
Albany, New York
Sly, P. G.
29 St. Andrews Avenue
Grimsby, Ontario
CANADA
Smith, H. M.
(Deceased)
Spencer, J. W.
(Deceased)
Stewart, Ronald
Atmospheric Science Research
Center
State University of New York
1223 Western Avenue
Albany, New York
Storr, J. P.
Biology Department
State University of New York
Buffalo, New York
Straw, A.
(Address Unknown)
Stupart, R. F.
(Deceased)
-192-
-------
Sutton, R. G.
Dept. of Geological Science
University of Rochester
Rochester, New York 1^627
Sweers, H. E.
Canadian Oceanographic Data
Centre
615 Booth Street
Ottawa 12, Ontario
CANADA
Sykes, R. B.
State University College
Piez Hall
Oswego, New York 13216
Taylor, B.
(Deceased)
Taylor, P. B.
Department of Mathematics
Manhattan College
New York, New York
Taylor, P. A.
Department of Mathematics
University of Toronto
Toronto, Ontario
CANADA
Thomas, J. P. J.
Canada Dept. of Mines &
Technical Survey
Ottawa, Ontario
CANADA
Thomas, M. K.
Climatology Division
Meteorological Branch
Department of Transport
Toront o, Ont ario
CANADA
Thomas, R. L.
Canada Centre for Inland
Waters
P. 0, Box 5050
867 Lakeshore Road
Burlington, Ontario
CANADA
Thompson, J. H.
Department of Geography
Syracuse University
Syracuse, New York 13210
Touvell, W. M.
University of Toronto
Royal Ontario Museum
Toronto, Ontario
CANADA
U. S. Congressional House
Committee on Foreign
Affairs
Washington, D. C.
U. S. Department of Interior
Pish & Wildlife Service
Ann Arbor, Michigan
U. S. Department of Interior
Federal Water Pollution Control
Administration
(now)
Federal Water Quality Adminis.
Great Lakes Region
Chicago, Illinois
U. S. Geological Survey
Washington, D. C.
Upchurch, S. B.
Department of Geology
Michigan State University
East Lansing, Michigan
Upham, W.
(Deceased)
Vanderpost, J. M.
Dept. of National Health &
Welfare
Public Health Engineering Div.
Bacteriological Laboratories
Kingtson, Ontario
CANADA
-193-
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Verber, J. L. Wright, G. P.
Northeast Marine Health Lab (Deceased)
Building S-26 C.B. Center
Davisville, Rhode Island yu, S. L.
02854 School of Civil Engineering
Cornell University
Watt, A. K. Ithaca, New York 14850
Ontario Water Resources
Commission Zenger, D. H.
135 St. Clair Avenue West Department of Geology
Toronto 7, Ontario Pomona College
CANADA Claremont, California 91711
Webb, M. S.
Meteorological Service of
Canada
315 Bloor Street West
Toronto 5, Ontario
CANADA
Weller, H. S.
Canada Center for Inland
Waters
P. 0. Box 5050
867 Lakeshore Road
Burlington, Ontario
CANADA
Weist, W. G.
U. S. Geological Survey
Federal Building
Albany, New York 12201
Whittlesey, C.
(Deceased)
Wiggin, B. L.
(Address Unknown)
Williams, E. T.
(Deceased)
Wilshavr, R.
U. S. Army Corps of Engineers
Detroit, Michigan
Woodrow, P. L.
Hobart & V. lliam Smith Colleges
Department of Geology
Geneva, Nevj York
-194-
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Aerial ice observations and reconnaissance, the great
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Bakewell, R. 1847. Origin of the Whirlpool and Rapids
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Bajorunas, L. I960. Littoral transport in the Great Lakes.
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Bubec, R. C. 1970. Water temperature and dissolved oxygen
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VI, ACKNOWLEDGEMENTS
We would like to thank the librarians and scientists
without whose assistance this compilation would not have
been possible. We are particularly appreciative of the
cooperation by Donna Browning, Elizabeth Robins and Ruth A.
Sparrow of the Buffalo Museum of Science; Emma Posdick of
the Canada Centre for Inland Waters; Rhea Bush of the Erie
County Public Library; Ruth Rehfus of the Great Lakes Lab-
oratory of the Bureau of Sports Fisheries and Wildlife (Ann
Arbor); Albert Ballert of the Great Lakes Commission; Jean
Seddon of the University of Toronto; Delloss Matheson of the
City of Hamilton; Arthur Pinsak of the U. S. Lake survey and
Andrew Robertson of NOAA.
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«US GOVERNMENT PRINTING OFFICE 1973 514-154/282 1-3
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SELECTED WATER
RESOURCES ABSTRACTS
INPUT TRANSACTION FORM
/. Report No.
4. Title Annotated Bibliography of Lake Ontario Limnological
and Related Studies - Vol. Ill - Physical
7. Author(s)
Baldwin, John and Robert A. Sweeney
9. Organization Great j^kes Laboratory
State University College at Buffalo
5 Porter Avenue
Buffalo, New York 1^201
12. Sponsoring Organization Environmental Protection Agency
IS. Supplementary Notes
Environmental Protection Agency report
number, EPA-R3-73-028c, March 1973.
3. Accession No.
w
5. Report Date
6.
8. Performing Organization
Report No.
10. Project No.
11. Contract/Grant No.
16120 HVR
13. Type of Report and
Period Covered
October 1971 - Jan. 1972
16. Abstract
Four hundred thirty-nine (^39) papers concerning physical aspects of Lake Ontario
and influent tributaries were reviewed and abstracted. Each paper was cross-
indexed by author, geographic area of lake and/or tributary in which study was
performed, parameters, techniques and instrumentation. In addition, a list of
addresses for the authors and agencies was included along with other possibly
pertinent references which the authors were not able to secure and review within
the time limitations of the grant.
17a. Descriptors
17b. Identifiers
17c. COWRR Field & Group
18. Availability
19. Security Class.
(Report)
20. Security Class.
(Page)
Abstractor
21. No. of
Pages
22. Price
Send To :
WATER RESOURCES SCIENTIFIC INFORMATION CENTER
US DEPARTMENT OF THE INTERIOR
WASHINGTON, D. C. 20240
Institution
WRSIC 102 (REV JUNE 1971)
5PO 9 I3.26f
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